acta gaologlea polonica
Vol. 23. No. 1 Warszawa 1973
MICHAL SZULCZEWSKI
Famennian -Tournaisian neptunian dykes and their conodont fauna from Dalnia in the Hol!} Cross Mts
ABSTRACT: Neptunian dykes containing a unique fossil assemblage were found in ' the Upper Devonian limestones of a l'eef-oomplex on the Dalnia HiLl in the Holy Cross lVIts. Fissures df'the tectonic origin were opened and filled under subaqueous conditions. The cOIlodont fauna they 'oontain indicates that a repeated filling and re-opening of the fissures took place in the Famennian and Toumaisian. The filling of a main dyke and ,the fauna it contains correspond to a condensed sequence depo sitedona submarine rUle. The reconstructed outline of the area of a condensed sedimentation ,in the Famennian and TOlll'naisian approoximately coincides with the outline of a dead Frasnian table reef. The trace of fa'cial boundaries in the Upper Devonian and Tournaisian is toa considerable degree determined by a 'block-faulting simultaneous with 'the sedimentation. The facies pattern here presented seems to exert a 'certain influence on la'ter, pc:Jst-Carlboni:ferous tectonics. The paleontological part of the present paper inc1udesa systematic des'cription of 29 conodont'species, mostly Tournaisian ones, which have not so far been described from the Lower Carboni- feroous of the Holy Cross Mts.
INTRODUCTION
In 19:68, a new locaHty otf abuillldant and unique fossil fauna was disCOV'eTed in the 'course of work on the stratigraphy and sedimentation of 1lhe Upper !Devonian in the'WesteT1Il /part of the Holy Cross Mts. The locality is situated in the western part of the Kadzielnia range otf the Frasnian, at the Dalnia Hill 0IIl the .outskirts of Kielce. This Frasnian chain belongs to the southern limb of the Kielce syncline 'connecting it With the Dyminy anticline ,
quite new taxa and, on the oth€l', its nearly entire fauna occurs in a spe cific geological situation as it is contained in a neptunian dyke. The presence of :the neptunian dykes rich in fossils throws a new 'light on several general, 'Paleogeographic and pa:leotectonic problems. The malIlil1er. of tthe occurrence of fossils iJ:l~nders, however, to a considerable extent a stratigraphic analysis and in -a way decreases the ·stratigraphic impor tance of the find. The material of the dykes does not display a distinct stratification and fauna varying in age is mixed in it, Famennian and TOUI'naisian forms occurring as well among the fossils. In 1969'-1971, these fossils were exploited by the writer and, partly, Doc. A. Stasiilska from the Polish Academy of Sciences. The elabOration of the material collected was .UIIldertaken Iby specia'lists from the Paleozoological Insti tute, Polish Academy of Sciences. A considerable pa-rt of the paleonto logical materials has already -been studied and their desoriptions are being publiShed in the present volume of the ACTA GEOLOGICA POLONICA (Osm6lska 1973, Stasiilska 1973, Fedorowski 1973). Docent H. Osm61Slka elaborated the entire collection of trilobites and Docent A. Stasiilska all the taibulates collected. Docent J. Fedorowski's paper oonceI'ns only part of the rugose corals. The rest of them, about 1,500 specimens, remainiJng at the disposal of Professor M. R6zkowska and Docent J. Fedoro'Wski, will be successively presented as further parts of the deseription .of fauna from DaItnia. Relatively few holothurian sclerites from that locality, have enriched a collection which makes the subject of a separate description, also in the present volume of the ACTA GEOLOGICA POLONICA (Matyja, Matyja & Szukzewski 1973).
. Acknowledgements. The wdter's thanks aTe extended to Docent H. Osm6lska, Docent A. Stasinska and Docent J. Fedorowski for their taking the trouble IOf -the description of fauna from DaJ.nia and for a discussion of stratigraphic and facies problems dealt with in the paper. The writer feels also indebted to Professor M. R6z kOWS'ka, now elaborating considerable part of corals from Dalnia, for giving pre liminary information on w'hi'Ch 'Chara NEPTUNIAN DYKES The neptunian dykescontainilng -a rich faUlIla occur (Fig. 2) in the top of the Dalnia Hill. They appear in a section which approximates the horizontal one and, therefore, they are visiJble "in plan". The dykes are well exposed as the result of the exploitation of limestone ina small rural quarry. Unfortunately, the exogenic ·a01d exploitation processes removed considerable part of the dykes. The neptunian dykes (Fig. 2B) cut through the Upper DeV'OlIlian oolitic limestones, Which aTe thkk -bedded and have dips of 30° and strike of 32°. The dykes run in principle ACTA GEOLOGICA POLONICA, VOL. 23 M. SZULCZ.EWSKI, FIG. 1 . A B o 1 2 3 4 5km I General map of Poland (A) and geological sketch map (B) of the western part of the Holy Cross Mts (after Czarnocki, 1938; simplified _ cf. Szulczewski 1971, Text-fig. 1) showing location of the Dalnia Hill (arrowed) and other sections dkcussed in th present paper (bold-faced). The remaining profiles and iheir abbreviations are the same as used in the previous paper (Szulczews:k:i 1971) I Cambrian, Ordovician and Silurian, 2 Lower and Middle Devonian, 3 Frasnian (fT) and Famennian (fa), 4 Lower Carboniferous, 5 post-Varlscan cover (Zechstein _ Upper Cretaceous) NEPl'UNrAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 17 parallel to the strike of oolitic 'limestones and penetrate them nearly vertically. The ll1etwOl"lk of dykes consists of two main dykes parallel to each other and separated bya 50 cm .- wide ledge of the oolitic limestoll1e cut by several small ;perpendicular dykes (Fig. 2A), 'which vary in width within limits of severa·l scores of centimeters. The smaUdy'kes are a few mm 'to a few cm wide. They are tortuous and either cOIl1nect the two main dykes, 'Cutting through the oolitic limestone of the ledge which divides them, or penetrate into the outer parts of this limestone. The fissures are filled with: (1) a pink to green marly limestone; (2) a gray crinoid limestoll1e; (3) a gray-g~een organodetritall limestone locally containing intTa clasts of a pink marly limestone; (4) black and alive-green clayey shales. A . . 'e': ...... ' .' .' :. : . : . '. . '. . ~" ...... : '., . o fm I I Fig. 2 Sketch plan of the outcrop (fragment) with neptunian dykes (A) and magnified section (B -atlong k-m in A) through the oolitic iimestones cut by neptunian dykes at Dalnia 1 ool.j.tic limestones, 1I neptunilllll dykes, :I calcite veins; circled numbers denote the conodont samples 2 18 MICHAl. SZULCZEW·SKI . The clinoid limestone has been found only as a small lens sep,ara tely emlbedded in oolitic limestones (Fig. 3). The clayey shales have been found only in the waste. On the other hand, the pink or greenish marly limestone is absolutely predominant in the filling of both main dykes. In the northern dyke it is the only type of deposit, but it does notcOtntain any macrofOSSils, which OICour, however, in the limestone of this type in the southern dyke (corals, brachiapocis, 'trilobites, cephalapods). The marly limestone a'lso makes up a filling of all small dykes. The gray-green organodetrltallimestone, probably exploited already, occurs in very small amounts. Most specimens come from the waste, that is, 'a 'limestaneoonsistitug 'primarily of fragmentary trilobites and a crinoid detritus, with intraclasts of a pink marly l:imesoone, identical with that described above, which are embedded in it. The houndary between the two rocks, although visible in detached blocks only, is distinctly sedi mentary (erosional) in character. It also indicates that the organodetrital limestone is older than the marly one. The filling of the main southe:rn dyke prohably also contained at first a thin 'layer af red clay ahoundinlg in 'corals, as indicated by a rich occurrence ofexcel'lently separated corals accumulated in one place in the waste. It seems very unlikely that they could be so accurately sepa- o 10cm L....--....J Fig. 3 Detailed section showing position of thecrlnoid limestone in the neptunian dykes at Dalnia 1 oolitic limestones - bedrock of the ,neptunian dykes, 2 crinoi GENERAL CHARACTERISTICS OF THE MACROFOSSIL ASSEMBLAGE ConodOllits and corals make up a preddminant element of the collection under study, with trilobites being also abundant. Other fOssi'ls as cepha'lo:poids, brachiopods and· crinoids (except for a lens of crimoid limestone) are ~are. Concise cha:racteristics O!f individual groups, in parti cular corals most of which are now only being studied, wiN he presented as follows. Corals. Rugose and 'tabulate corals, as wen as heterococals are present in the ,collection. The first of them make up about 90 per cent of a'll corals. The heterocorals are the least numerous and rugose corals occur only as so'litaryforms. No calonialforms have bee:n found. For this reason, as weN 'ag due to their smaN size and lack of dissepiments, they are of the type of the Cyathaxonia fauna (sensu Hill 1938, p. 5). The genera Cyathaxonia Michelin, N eaxon Kullmann, Pseudomicroplasma Soshkina, as well as metriophylloid, and cystophylloid forms predominate among them. The forms mentioned above were :rare among the corals previously described from the Famennian of the Holy Cross Mts (R6z kowSka 1968, 19'69). And on the contrary, the genera Petraiella R6Z kowsika, NalivkineUa Soshlkip~ alIld the forms assigned to the family Kiel eephyllidae and +.0 the order Heter'OCora'llia are rare at Dalnia. Particu larly important is a rare occurrence on Da:lnia of the genera, which in 6th~t outcrops (R6ZkOwska 1969) aippeared only in the lower part .of the Famen'nia'l1, e.l. Petraiella R6z,kawSka. Kielcephyllum R6Zkows'ka, Koz1.owskinia R61JIrowska, N alivkinella Soshltina. There are 100 represen tatives Of the superlfamily Phillipsastraeidae common in the Frasnian and very rare ID the 'lower part of the ,Famerunialn. Instead, there 8(ppear new genera and several mew sp,ecies of the :families Metriophy'1I1dae and Lacco phyllidae. The State of preservation of the corals :is variable. Excellently preserved are the representatives of the subfamilies Metrioppyllinae and CyathaXlOIlllnae. Specimens of some . genera (e.g. PetraieUa R6iJkows'ka, Amplexocarinia Sosbkina, Gorizdronia R6zkowska andcystophyllid forms) are, on the other hand, frequently broken and, as the result of recrystalIizatiO'll, with a poorly preserved internal structure. Tabulate corals aTe assigned (Stasiilska 1973) to the following gene ra: Emmonsia Milne-Edwards & Hairne, Michelinopora Yabe & Hayasa ka, Acaciapora Moore & Jeffords and KueiC'howpora Ohi, which have hitherto not heen known from the Holy Cross Mm. All species are new. These are without any exception small forms, coITeSJ>Onding in dimen- MlCHA~ SZULCZEWSKI sionsto rugose' corals which ,they accompany, and aTe spherical, either c1Ulb-or Ibranch~aped. Trilobites are also the subject of a separate elaboration (Osm61S'ka 1973). In the ,co!llection they are rePresented by 12 spe'cies and su'bspecies of six genera. One 'Of them is clearly Devonian in ·character (Phacops) and four Cartboniferous (Globusia, Phillibole, Carbonocoryphe, Liobolina). Most species are new. All trilObites are small. A high vaulting of ceJpha Ion, swoaen genal spines and advanced reduction of eyes (Osm6lSka 1973), displayed Iby several species are considered the m'Ost striking charaders of the assemlblage. Ammonoids are very raTe; they are represented by a few fragments of Woc:kLumeria Sip. only. THE AGE OF INFILLING There are two fundamental factors which make difficult an exact determination of 'the age 0If the neptum.ian dytkes on the Damia Hill and of the fossil assemlblage theyoontain. The first is a genexaUy observed mix!i!n:g of fauna varying in age and tlhe second ~ the lack of stratifica tion and a deifiInite spatial orientation in the infilling of fissures with a simultaneous lithoLogical simi1arities of deposits varying in age. Of the fossiils contained in the dykes, conodonts are of a fundame'ntal impor tance. A 'common assemblage ofabUlIldantly represented species, having narrow stra'tigraphic ranges well-known for most of the species, is deci sive in this respect. The trilobites play an accessory role but they do not wovide a possilbility of such a precise stratigraphic d~vision as do the oon odonts. They are incomp,arably less numerous and most of their taxa are new. Due to theiT extensive stratigraphic ranges, usually not yet deter mined definitely and a great number of their Illew taxa, 'corats play here a small stratigraphic Irole only. In (practice, the age of coraiIs and, to a considerable extent, new species of trilObites is indicated by the assem blage cif associated conoclonts (Table 1). Thus, the nomencl.atture of the biostratigraphic units iI"epresented :iJn the fissure infilling has been /based on the conodont standard zOnation. Some of the conodont samples contain a unfform-age assemblage and referring them to appriopriate oonodont zones does not poSe any problems. In !mixedconodont ;faunas, elements coming from know'n ZOIIles have been determinea only as [a'l'as posstble on the basis of known ranges of species. Conodont zonation. 'J'Iherecanstlruction of stratiJgraphic conditions in the neptum.ian dykes on tlhe Da'hrla HiU (Fig. 4) is p,ossi'ble only due to a considerably advanced knowledge of the Upper Devonian and Lower Ca1"bonilferous ACTA GEOLOGICA POLONICA, VOL. 23 M. SZULCZEWSKI. Table 1 Distribution and frequency of conodonts and associated fossils in particular samples from neptunian dykes at Dalnia Samples 6 1 6&.1 7 1 819 1101 11111BI 12.I12BI 1JI a I b ! a Id le It 1 .. Ior1odu8 alternatua BranaoD a: If.hl ...... Icr10duIS oornutu8 SanneDl&ZlD ...... Nothogrns,thella of. postsublaeT1s Belma a. .claka ':1 I 11 1 1 I Nothogilathella/?/ falcata H.lm. • ••• g Palmatod.lla d.l:I.oatula Ulrioh /I; Basal.r • 2 141 I 1 " : Palaatolep18 d1.itorta BransoD et )iehl ...... 8, 7 & 9~ 9 1 I ' I I ~ Palmatolep1s glabra Iepta Z1egler &. Huddle 141 JO 2& 420 '1131 1 I' 1 i Palmatolap1s glabra pect1nata Z1egler .. .. 1 :: Palmatolepls g.l"B0111.8 graol11s BraIUlOD a:. "ehl - 16 Palmatolup1a m1nuta m1nuta BranaoD 4. Mehl • .. • I :~;' j, ~II 31 1 8 I 1 'I' Palmatolep1tJ perlobata perloba.ta Ulr1ch A Bassler icl' Palmat~lep18 quadrant1nodoaa marg1nlle:ra Belms 4744"13 68110 ,,1I 1 1 1 I 1' I ~ Po17gnathus of. flabellu:s BransDD a. )jahl .. 1 I I E Polygnathu:I glaber gl.l3.ber Ulr1.oh 4:; Bu~ler 2. 27111 I I I I $ Pol;rpathua glabor bllobatu.. Ziegler • • J 1 2 2. 1 1 I 1 ! Polypathua gloMr lIIediua· 8elm. & lIo1aka • J I 11 '" :! Polygnathua lagow1ens1s He1mz; 4. Wolaka .. .. 1 I I I I PolJ'gnathus DodooOBtatU8 nodooostatua Bransoll 4; Mehl I 2' 171 21 1 1 1 I' I !, POl;rg.DathU8 nOdo.undatuB. 8elmB •• • • • • • 1 1 11 ]1 Pol;rgnathua perple""s /1!!la ...../ • • • • • • • • • • • I 6 1 1 I I, P~iil;;pho.i~Dt;.luigu:iio~U; B:rano~D .t. lI~hi . . . • • 1 7 21 I .n••• ;.'U •••• •. •••••••••••• 1... Palma'-olopia·~"".'.UD gon1oolym.n1 '.".'=~'=".""".'.'''.'.... lIullor • • • • I... I' .. j".r ...2' L"".~ t I ... I'=' '... I.=.t.J I lit .. =t .. =... • ~:I 'almatolepia graoll1a .. aigmoi~l1s Z1egl.r : 1 121 I' I I I 21 1 J 1 .. o 0 Paaudopo17gnathu8 tr1gonioua Z1egler • • .. .. 2 I 1 1 , .. :5" Spathognathodua aoul.atuB /Dranson& Mohl/ • I, 2 2.1 I 2. I 2. ! ~~ ·Spathopathodus costatus aostatus /B:ranBon/ • • •• 91 8 1 I 1 78 I, I 41 21 1 6 '1 10 I 13 11 I I) :5 '.: Spathognsthodue cost&tUB 'pinul1oostatu8 /Bro.nson/ 2\4 I 24 1 2 l' 6 111 11 j 1 8 .., !:: Spathognathodus o.status ult1lllus BiachoU ! 2 1 I , . " Sp~.;tb.ognathodul!5 8upremua Z1aglor • • • • • • • • • • 12 6 I I 2 1 4 1 I 6 :3 I '" .... ;:~=;:::.;::::::.::=:.;:::::=:.:::~ .. ~ ... =•• ;; a;; .. ztl ... ToszrJ;.tl-;~+"I"-'";T;;f;"I-" ,";;j";; .. Polypathus inOrna.tus Br"""o" • • • • • • 61' , 'I 1 21 11 I I 21 61 2 " ;., Pol;rgnathu8 longipo.tious. Bxanaon & lieU. J 4 1 I 21 I I I' u ::.1! POl.TgnathU8 8,TDIIDatr1cU8 Branson • 2 I 1 1 I I 1 'I 1 !; Polygnathus Tog•• 1 Zi.g1er • • • • ) J 1 11 2 1 1 I 9 1:1 Protopathoduo coll.1nooll1 Z:I..glor 1 11 1 1 I 1 1 ~.:t Protognatbodua u:eischneri. Z1.egler 1 I I ~ B Protopathodua kockeU /Discho:l:l/ 2 J 1 1 1 1 I 'I ~! ' .. udopol,ygnat!lu•. deDt111noatua Branaon 6 21 I I, I 1 I 1 ! J I ~ '.eudopolygnathua Dodomarsinatus /Bru.aon/ 12 I ! J I 8 9 "' Spathognathodus dispa:!"1l1a /BransoD & lIehl/ Spat!l·>gnathodu. stablli. /Dranaon .t. lIeU/ • .... .,...= __ =.. ".,.."'...... : .....u ••:Il=<=- ...... ,,;.:; .....c ..."":;a ..... DinoduB wUson1 Druoo •••• •. ; 1 I I· 1 I I 1 1" 'I" Polygnathue oommu.nJ.s oar1.nus Bass ... JI 11 1 1 1 ). i 181' Polygnsthus purua purus VogeB •• 27 12 I 41 41 41 1 11, 2 2! 41 2 Polygnothua purus subploDua Voges 10 1, , 6 21 I )1 2 I 1 1) 14 ~ 'aeudopol;rgnathus tusiform1a Branaon & lieU I 2 , 21 ~, 11 1! 1 1' I 2 ~ Pseudopol;rpathus marg1n&tua /BranaoD & lIehl/ 2 I 11 I ! I I !l Ps.udopolygnathus pr1mua BranoOD & 1I0hl •. • 9 l 11 2 I! 1 '21 ;, 3 P•• udopolygnothua tr1angulus p1nnatus Vogoa 21 I " I JI I 'I 11 I ! 'a.udopol;rgnathus .p. A • • • • • • • • 21 2 2 ~ 'seudopol;rpathus sp. B •• • • • • • • 3 1 11 I I :: S1phonod.lla dupl10ata /Dro.nson & lIohl/ 191 11 1 ! I 1 Jl4 1 81 I, 41 9 1, 6 SiphoDOd.lla lobsta /Brsnaon .t. lIeU/ • • I I 1 1 1 ' S1phonodello ob.cleta Bass. • • • • • • • 1\ 1 I 1 2 11 2 I I Siphonod.lla qundrupl1cata /Branson & M.U/ 2 I 3 1! I I 2 2 •••••• .1...... =.: =!tl=- ~:e~!~~!:~.~~:~!~.~~~:!~Phaoops .x gr. granulatua •• :.:.~.:.;.:.:.;.:..:.:.• • • • • • • • • •• ~.~L.~Lso~I I x 't... j.. .l.zef···l.···I I ! ·!~···I···~·z 1 ' .. =.~.a!L.I' 3 lIaribolo app. • • • • • • • • • • • • • • • • • x I I I ! I I, 1 I .. IUobua1a d1fiortigena /Os1II61ska/ • • • • • • • I' I 'I I, x ~ Ph111ibole drewer..,..ia latipalpebrata Os ..61Bka • •• x I 1 I I 1 1 xl xl x ~ Phi11ibole nitida annosa Oa.6lska ••••• • • • • I' I I, 1 x Ph1111.bole prenes Osm61ska ...... • • ...... • x C;yathaxoD1& oo,'"u Uioholin • • • • • • • • • • • • • I I I' 11 I I I C;ratllaXon1& sp. •••••••••••••••••• I 'I' 1 1 I Hlllaxon .,.siculosua R6tko... ka I 1 1 • lieaxOD regulu. /Richtor/ • • • I ! I I. , 1 1 ,3 I ... l/eaxOD Bp. ••••••• i I I 1 I I III Petra1ella centraliS R6tlcoW'sk& .. I J4 Petra1ella kleloens1s R6tkowska I I. ',' I 1 I i Sal•• laa.... ap. ' , I I I 1 ~ I u Smith1pQllum sp. I I 1 I I 1 1 i Sir1ngaXon sp. 1 I 1 I I, " aenua DOT. , ! I 1 I 1 I Aoao1.apora 1nfraoarboD1oa Stu1f1aka ...... t 1 ~:l::::r=ti;;::d~·;;bh:~~;;:·G:b;h~;k;·C:;;:;·;·B;1ii·:·:· . ;;, ••• ll··· ... zl···t·=r-I···~·.ll z·t··+·+· OCl·· ·.J··· Bocaud1no of. hoxagolll!- Kri.tan-'l!ollDlann • • • • • 1 I I I I I 1 I I I Determination cl. the · rugose corals by Professc»:" Mo R6tkowska (pcq)eT in PTepflTation), tabulate corals after Stasiflska (19'13), trilobites after 0sm6lska (19'13), and holothurian sc:lerites after Matyja, Matyja & SzuicZewski (1973). Numbers of the trilobites not given as these are preserved as disarticulated parts of exoskeletons. Of the macrofossils, only the forms identified in the conodont-bearing samples are given. Numbered samples come from the neptunian dykes (cf. Text-figs 2r-3), lettet"ed ones come from loose blocks (waste of the dykes) containing the macrofossils • Palmatolepis graalis ymcais Branson & Mebl may belong either to the assemblage from the Palmatolt!pis quadrantinodosa Zone or from. the Spathognathodus costatus Zone l> NEPTUNJ'AN DYKES AND THEIR CONODONT FAUNA FROM DA'LNIA ~l: conodont stratigraphy. On a world scale, Upper DevOiIlian conodont zo nes are of a universal character. The successian and definitions of their zQIIles have Ibeen adopted aOOOO'ding to generally ac'cepted principles in troduced by Ziegler {1962, 1971). The stratigraphic division of the Lower CarIbonifeirous based on ,oonodonts is not, however, so un1tform which seems to resu1t in par,t from the existence of provinces. Due to the simi larity of the conodont tfauna and relatively strongest region~'l relation ships, the conodont ,zonation has, therefore, been based on Voges' (1959) succession. Upper Palmatolepis quadrantinodosa Zone (to IlIa). - The distin guishing of 'this ~zone is possible mostly on the basis of evolution within the Palmatolepis quadrantinod08a and P. glabra (Ziegler 1962, pp,. 31 and 33, Table 2; 1971, Chart 6). The abundant occurrence of Palmatolepis quadrantinodosa marginijera Ziegler, with a simultaneous lack of the remaining subspecies of P. quadr,antinod08a, indicates that the assemblage they are conta:iJned in represents the Upper P. quadrantinodosaZone. 'l\he same condusion is suggested by the mass occurrence 'Of Palmatolepis gla bra lepta Ziegler & Huddle, accotmpanied by P. glabra pectinata Ziegler and P. distCYrta BransOlIl & Mehl, with a simultaneous lack of P. glabra prima Ziegler & Hudd.le and P. glabra acuta Helms. Also present are the polygnathid species Polygnathus glaber bilobatus Ziegler and P.' lago wiensis HeIlms & Wolska, which are not known in higher !beds than the Upper P. quadrantinodosa Zone (Zieg'ler 1971, Chart 6). On the other hand, except for a single transitional form from P. perlobata to P. rugosa gr08si Ziegler, no Palmatolepis rugosa subspecies diagnostic 'for this zone has ever been IfOlUIld. Ziegler (1962, p. 33) ascertains, however, that this species, is not frequent. This is confirmed 'by a 'low frequency of the subspecies of P. rugosa in Wolska's (1967) collection from the Holy Cross Mts. The remaining species found in the samples referred to the Upper Pa1matolepis quadrantilnodosa Zone belong to typical and common ele ments O!f this zone, although they exceed it in their ranges. Noteworthy is the presence of Polygnathus glaber medius Helms & WolSka. SamPles 7 to 10 '(Ta1ble 1) may be surely referred :to the Pahna tolepis quadrantinod08a Zone. They are sufficiently abundant (a total of about 2000 specimens) to give the certainty that they make upa represen tative materia'l devoid of any admixtures of another age. Very characte ristic is quantitative predominance of Palmatolepis glabra lepta in all the samples. Specimens belonging to this,species make 'Up more than 60 !per cent of the entire collection of Palmatolepis coming ftrom thls zone. Middle Spa,thognathodtus c08tatus Zone (to · ?V/VI-VI) . . - Only one (No. 11) sample, devoid of the· elements of another age, c~leiely represents this zone. It is not abundant, but contains an assemblage very cha!racteristic oif this zone (Ziegler 1962, p. 41, Table 2; 19'71, Ohart 6) . . It includes Palrnatolepis gonioclymeniae Miiller, the, only species mown, .. UPPER DEVON/AN LOWER CARBONIFEROUS .... ~ ';"'Manticocerasl Pericyclus e..§ 0;. ~ o I tI ~. a.... f3. 0 ~. i i 10 cm I a ~ ~ <+ 0Cl :;J' • 8 III ~ ::s ~ 03 t".I 8" ~. ~ ::s 0. ~ III 10'" rl- tj i ~NIAN DYKES AND THEIR Co.NODONT FAUNA FROM DALNIA 23 the range of whioh is confined to. the Middle Spatho.gnathodus costatus Zone. ConcU'rring with it are Spatho.gnathodtus costatus ultimus Bis choff, S. supremus Ziegler, Pseudopolygnathus nodomarginatus (Branson) nad Pseudopolygnathustrigonic:us Ziegler, whose ranges are limited to the Middle and Upper S. costatus Zone. The appearance o.'f the first of them together with P. gonioclymeniae determines, according to Ziegler (1962, p. 41), the !base of the Middle Spathogna'thodus costa-tus Zone. Th€l'e also occUlr several other species ,common in this zone, but with more extensive stratigraphic ranges which include Spathognathodus costatus costatlus (Branson) and S. costatus spinulicostatus (Branson). The OQIlcept of the last two species, conformable with Ziegle;r's (1962) views, has here been accepted for the reasons given in the remarks concerning subspe cies, discussed above in the paleontological part of the present paper. The To.urnaisian conodont zones. - The Tournaisian .conodonts axe very abundant in the infilling of the fissure, but they occur either in mixed assemblages, or are so few in the samples that such a mixture cannot; !be precluded due to the insufficient fu"equency in the sample. Mixed 'faunas correspond to a considerable stratigraphic interval. Accom panying the species irOlIll the upper part of the Tournaisian, there occur not only the forms from the Lowell' Tournaisian but also from the Middle Spathognathodus costatus Zone and even from the Upper Palmato.lepis quadrantinodosa Zan'e (salnple 6A). Under such 'circumStances, distin guishing particular conodont zones of the TOUTIlaisian is dbvio.usly im possible. Nevertheless, we can reconstruct the interval of the Lower Car boniferous 'to which the whole of the mixed fauna's correspond and the zones from which approximately come the elements of which they are composed. Species of the genus Protognathodus are among the oldest fwms. Pro.to.gnathodus co.llinsoni Ziegleil', P. meischneTi Ziegler (= Gnatho.dus Bp. A of Collinson, SCo.tt & Rexroad) and P. ko.ckeli (Bi~hoff), present on the Dalnia Hill, are the ,chief components of Ziegler's (1969) "Proto gnathodus-Fauna" which occurs in the uppermost Late DevonianOlf Stoc kum and Seiler (Ziegler 19'69; Ziegler & Leuteritz - in Koch, Leuteritz & Ziegler 1970) betWeen the Upper Spathognathodus costatus Zone (to. VI) and the Siphonodella sulcata - Protognathodus kockeli Zone (cu la). In SrockulID (Weyer 1965), it is a'Ccompanied by Pricny.oceras (Imito.ceras) sub striatum, P. (I.) carinatum and P. (I;) prorsum and the position of the "Pro tognathodus-Fauna" corresponds in the standard profile of Honnetal to I~he upper part of Hangenberg Schiefer (Ziegler 1969, Abb. 2; Austin & a!. 1970; Bender & a1. 1971). The range 0If lIlone of the species of Protognat hod:us is, howeve!l', limit~d to the interval with the "Protognathodus -Fauna". They a'lso occur in the Lower Tournaisian (Ziegler & Leuteritz - in Koch, Leuteritz & Ziegler 1970, Ta:ble2). Since on the Dalnia Hill, specimens of Protognathodus occur among mixed faunas, the settlement MICHAl. ·SZULCZEWSKI of the question whether they come from the uppermost· Late Devonian or !from the Lower Tournaisian is impossible. . The genera Siphcmodella and Pseudopolygnathus present at Dalnia are of a particular importance to the stratigraphy of the Tournaisian. The ppylogenetic development of these genera provide a basis for the cono dontzonation. The presence of Siphonodella sulcata (Huddle) seems to indicate that the conodontsfrom the Siphonodena sulcata - Protognat hodus kocikeli Zone (cu la) of the surely 10wermost zone OIf the Tournai sian are present in the mixed fawnas. This species, also tr;elated to the genus Polygnathus,is the oldest phylogenetically and makes up an ance stor of the young,er Siphonodella. The species S. duplicata (Bransan & Meh'l) , derived from it, ailows to state the presence of conodonts coming from the next zone, i.e. Siphanodella - PseudopO'lygnathus triangulus inaequalis Zone (cu la/{J). On the other hand, it is difficult to decide whe ther the elements of the next two zones, Siphonodella - Pseudopolygna thus tr'iangulUs triangulus '(CU 1{J) and Siphono'del1a crenulata (cu 1/11 - cu l1a), are pres'ent or whether only the upper 'one of the two ZOIIles is represented. Siphonodella quadruplicata I(Branson & Mehl) and S. lobata (Branson & MeW) are characteristic of these zones. Pseudopolygnathus triangulus pinnatus Voges and maybe also Dinodus wilsoni Druce are the youngest components of the mixed faunas on the Da1nia Hill. The former is parti'cularlycharacteristic and tYIPical of the Scaliognathl1lS ,am.choralis Zone I(CU II{J-r), but it also occurs in the upper part of the Siphonodella crenulata Zone (Voges 1959, Table 1). Specimens from Dalnia probably correspond to the last-named zone. Dinodus wilsoni has so far been known only froOm a type locality in Australia, where it occurs probably in the depOsits which make up an equivalent of this same zone (D:ruce 1969, pp. 24 and 54). The lack of the genera Scaliognathus, Doliognathus and Geniculatus, which appear in many European areas in the ScaUognathus anchora:lis Zone, as well as the lacJk of the genus Gnathodus, which appears some what earlier, dndicate that the entire TouTnaisian assemb'lage from Dal nia makes up a pre-anchoralis fauna, which correlates in the lCephalorpod zonation (cf. Bender & al. 1971) with the entire GattemJdo:ciia Zone and maybe also with the lowermost part of the Pericyc1us Zone (P. princeps & Muensteroceras oomplanatu'In Sulbzone). It is very likely that the sequence of the Tournaisiari faunas cor.,. responding to zones older than the Scgliognathus anchoralisZone is not rePTesented on ,the Dalnia Hill 'as a whole. The lack of late species of 8.ip1umodella, such as S. cooperi Hass, S. crenulata (Cooper), S .. iBosticha (Cooper) arnd S. obsoleta Hass, as well as Pseudopolygnathus triangulu8 triangulus V:oges '~d P. triangulu8 inaequalisVoges may be caused by the limit.ed BCOpe ,of theoollecti.on.o!l' Iby possible gaps. NEPTUNIAN DYKES AND .THEIR CONODONTFAUNA FROM DALNIA 25. Age of the coral fauna A dedded majority of corals has been collected from the waste. They probably come from a clayey deposit from which they were washed. Since it was pa'rt of the intfilling of the neptunian dyke 'containing de posits varying in age,aIn exact dating of these corals by means of other fossils is impossible. The determination of age on the basis of the coral assemblage alone also encounters ()Ibstacles. The stratigraphic ranges of the species of corals aTe very extensive and SO far insuffi-cen'tly studied as ,concerns the problems examined. In addition, there is no certainty that the entire collection is of equal age. Nevertheless, a SIDail part of speci mens come from the fragments of limestone, which could be dat~ by conodonts (Tal}jle 1). No dating of thds t~ indicated the Palmatolepis quadrantinodosa Zone. IIIl all cases, corals concurred either with an as semblage of the Middle Spathognathoduscostatus ZolIle (Cyathaxonici cornu Mkhe'lin, Neaxon sp.), or With 'an asselin!blage of the T'oUlnaisian conodonts (Saleesma sp., Petraiella kielcensis R62lkowska), or else with a mixed conodont fauna of the Spathognathoous com;atus Zone through the Siphonodella crenulata Zone. It seems, theretfore, that the 'corals :from Dalma, OT at least a predominaIntp,art of them, come from the uppermost Famennian (Spathognathod'llLS cOSitatus Zone) or from the Tournaisian conodont ZOIlles 'corresponding to the Gattendortfia Zone. The rare occu rrence in the Dalnia assemblage of the genera which are common in the lower 'Part -cif the Famennian (R6Zkowska 1968, 1969), With a simultaneous presence of marlk:edly Carboniferous fOflms, suggest similar cOIIlc1usions. On the other hand, a decided'ly Car:boniferous character is displayed by. e.g., Saleesma Weyer which has not 'been known from deposits older than the Gattendortfia Zone (Weyer 1970). Although ,new, the 'corals described Iby Fedorowski (1973) also seem to be younger then the Upper Devo niEm. The heteroco!rals are not very helpful in determining the ag'eof the assemblage. To be sure, until recently it has been recognized (e.g. Weyer 1967) that they appear immediately at the 'base of the ViseaIn, 'but R6z kowska (1969) found them also in the Famenm.ian. The tabulates Ibelong as a whole ;iJo new ,species and their ,genera. ex'Cept for AcaciapoTa, have their ranges widely exceeding the Lower Carboniferous. It is true that the Tournaisian age has 'been determined immediately by means of the accompanying conodonts on'ly for Aca:cia porra, ..but it seems hardly probable that they might l?'~ older than the Spathognathoduscostatus Zone, since they alw.ays accomp,any the tetra ~or Age of trilobites The occur!I"ence of trildbites in a limestone rich in ,conodonts allows one to date 'them by the last-named (Table 1). Of all these trtiloibites, Phacops granulatus (fMiinste!I") and Waribole sp. undoubtedly accompany the .assemlblage of conodonts from the Upper Pa'hnatolepis quadrantino dosa Zone (Table 1, sample 7); which is in conformity with the strati graphic Tanges settled for them. Nearly all the remaining species or sub species (Osm61ska 1973) are new, but belOiIlg to Lower Ca'l"'boniferous ge nera. Amy mO!I"e detailed examination of their age separate'ly from the fos sils accompany them is difficult not only on account of the newness of the species, 'but also on account of the inaccurate knowledge of the Lower CarbonifeTOUS trildbites (cf. Hahn & Paproth 1969, GandlI970). The genus Liobolina is characteristic of the Gattendoriia Zone, but at Zar~by neaT l.ag6w i(Osm6lska 1962) and at K6sten:hof (Gandl 1968, p. 507; 19700) it reaches the base of the Pe'ricyclus Zone ,(that is, the SiphO!Ilodella crenu lata Zone). The Species Phillibole drewerensis (Richter & Richter), formerly oonsidereld to Ibe restricteld to the Gattendor'fia Zoo'e, may also, very'ra rely, occur in youi:nIger (beds up to the Scaliognathus anchoralis Zone (Gan'dl 1968, W. 498-,499; 1970). CarbonocCYr1Jphe reaches still high eT strati graphically. On the Dalnia HiU, Phillibole drewerensis occurs either to gether with the Tournaisian assemlblage of conodonts or with a mixed assem1blage containing Toumaisian elelments, alang with those cOlming from the SpathognathodULs costatus Zone (Table 1). Such 'trilObite forms as Globusia differtigena (Osm6LSka), PhiUibole drewerensis latipal pebrata Osm6lSka, P. prenes Osm6lSka and P. nitida annosa Osm6lska, along with few conodon'ts re'presentilng the Gattendorlia Zone concur in one of the samples. Since the Tournaisian conodonts do not display a segregation corresponding to particular zones, we Should oonlfineourse[- . ves to the statement that these. four species come from the Ga ttendor'fia Zone or fTOlm the loweil"Inost Pa!I"t ,QIf the Pericyc'lus Zone corresponding to the conodont Siphonooella crenulata Zone. They are, therefore, older than ox at most of the same age as the trilobite fauna from Kostenhof and olde:r than the fa'lllIla from Geig'en (GandI1968, 1970). This is prolbaibily true as we11 of the Iremaining s~ecies and subspecies of the genera Car bcm.ocoryphe, Globusia and Liobolina. GENESIS OF THE NEPTUNIAN DYKES The infilling of the dykes is a relict of the youngest Devanian-Car boniferous sedimentary sequence presented on the Dalnia Hill. The de posits 'COrresponding to it are Illot preserved in a lIlormal sequence. The in fining of the dykes is, therefore, the onlysoUTce of information on the history of the Fame'lllIlian and Tournaisian sedimentation in this region. NlM'TUmAN DYKES A,ND THEIR CONODONT FAUNA FROM DALNIA 27 At the same time, this i'lliformation is incomplete and to a certain extent . modified by a specirfic ·behavior of the deposits. The calcareoU8~ar1y se dimenta'tion prdbalbly took plac'e herein tmoughout the Famennian and the Gattendorifia Zone. ':Dhe skeletal materia'l played in it an unequal role, the maximum role being manifested in the soo:iJmentation oif the 'CTinoid limestones. .The assemlblage of ['ossiIs may be termed as a coral-trilobitic one. The association dfthe Cyathaxania coral fauna with 'the trilobites is a common phenomenon in the CarIboniferous (Hill 1938), but on t!he Damia Hill there :is no third element - the brachiopods whioh usually accompany the two ,groups mentioned albove. TrilObites from Dalnia are comparable with the trilObitic fauna from what is known as "cephalopod -facies" (cf. Gandl 1970). ':Dhey include the representatives of the Bulbfa mi'ly CyrlosymboUnae characteristic of this facies, While Liobolina (now Cumminge'llinae, formerly CyrtosymboJ1nae) belonging to another family and a new geruus Globusia (Proe'tinae?) have, the same as the Crystosym boliJnae, reduced eyes and are small (Osm6lska 1973). Desp;ite a mass oc currence d:f specimens, the assemblage of rugose corals is distinctly of a non-reef ,character.. The fauna of Cyathaxonia is indicative of a calm water with a normal salinity (FedorowSki 1971) and it is typical of a soft, muddy bottOlIIl, covered with a very fine deposit. It corresponds to larger depths than the reef fauna of the same age. The tabulate corals, the same as rugose ones, are small forms and t!he development of characteri stic, narrow bases in Emrn,orn,sia dalniae Stasiitslka (cf. Stasiilska 1973, PI. 2, Figs 3 and 7) in contrast to overgTowing the rugose ,eora'ls without developing the Ibases (I.e., Pl. 3, Fig. 4) seems to be, the same as their small dimensions, determined by their growing on the soft, muddy bottom. The 'tri1olbites f·rom Dalnia display several adaJptative characters connecteld with their grdwiJng on the soft, muddy bottom. According to Osmolska (19'73), these are the reasons W'hich ,cause· their high vaulting ofcetpha1on, swollen genal spines and advanced reduction of eyes cha racteristic of most of the species. The entire fauna makes up in practice an assemblage of benthic or ganisms. Since ammonoids are ' very rare, only the abundant conodonts re'p1"esent the remains of nectonic origin. What is very ,characteristic is a great abundance of specimens oc curring in the neptunian dykes on the Dalnia Hill. This probably results from botIh favoralble conditions and a 10lW rate of depositioncorreswnding to the original sequence. The favoraJble conditions to the development of fauna are indicated not only Iby the albundance of individuals but also and primarily by the abundance of species and higher taxa. In this respect the fauna {)If Dalnia widely departs from some, only slightly differentia ted faunas described from other neptunian dykes (e.g. SchoU & Wendt 1971). The low rate of deposition may in the most obvious way be deduced . from the frequency of conodonts. Ln the Upper Devonian of the Holy . MICHAt. SZULCZEWSKI Cross Mts, :t!he frequency of oonodonts is clearly inversely prOlpOrtional to the rate of deposition. Such a highn-equency as that on the Dalnia Hill (300 and mOlre per 1 kg) is met with only inoondensed sequences in which the rate of deposition was particularly ,low (Wolska 1967, Szul czewski 19'71). All localities of an abundant Famennian ,coral fauna (R6z kowska 1967, 1969) also come from condelIlsed sequences, while they are exceptionally rare in the deposits otf basin fades varying in age. It is likely. however, that a certain importance should also be here ascr~bed to the sp.ecificity of sedimeD1tation in a fissure. Fossil-rich fiml'lgs O'f nep tunian dykes are verry common in the Triassic (Schlager 1969; Krystyn, Schliff.er & SClblager 1971; ZankI1971) and in the Mediter:ranean Jurassic (Sturan:i. 19'71, WeIIldt 1.9'71, ScholI & Wendt 1'971). The !faunas from the naptunian dykes are frequenftly tlhe most a:bUlIlidant in appropriate fomra tions. As noted by StuTani (1971), this seemingly paradoxical phenomenon may eaSily be exrplained by the fact that the fOlSSils were trapped within the open fissures, which made up the only places.where the fossils ,could escape further remO'Vai or destruction. The rtaphonomic character of the assemblage of trilobites contained in pink marly limestones might, according to Osmolska (19'73), indicate that the open fissure wasactuaHy a trap accumulating organic remains. The pink marly limestone contains fOrlIns representing various ecologic ada~tartions, whiCh indiICates a parautochthonous agglomeration af tr1ilo bite exuviae derived from the different environments. A complete lack of li:brigenae of Globusia differtigena (Osm61ska), which display swollen librlgenal spines, may be caused by hydromechanical factors (cf. Osm61- ska 1973) . . The gray orgSiIlooetrital 'limestone contains, on the other hand, an almost monospecific assemlblage of trilobites, in whiCh the exuviae of crSlIlidia, pygidia and the librigenae of G. differtigena occur alimost in proper proportions. This assemblage was deposited in the same site in which the moulting had taken 'Place i(Osmolska 1973). Since specimens of the gray organoidetrditai limestone were not found in situ, it :is impos sible to decide if they reached the fissure 'already after consolidation of the deposit 'Or were deposited in the dyke during the period when it was already nearlycomple,tely filled. . Thus, the original Famennian and Tournaisian sequence 'On the Da Inia Hill was formed under thec'Onditions in which a sudden arrest of subSikience and, cOiIlrSequently, 10'W'ering of the rate 'Of sedimentation were fav'Ora'JJle to tihe deve'lopment of the fauna under ~udy. The manner 'Of sedimentation in the Famennian and Tournaisian on the Dailnia Hill in dicates that it corresponds to a submarine rise, 'On which a condensed sequence developed. The f'Ormation oIf neptunian dykes which are correlated with the time of stratigraphiICioondensation following the reef sedimentation does NEPTUNIAN DYKES AND THEIR CONODONT FAUNA FROIM DALNIA 29 . not seem to be accidental The development of neptunian dykes over the reed: formations or carbonate platforms duoog the periods when the sub.,. sidence and sedimentatiOlh rates had come to ana'brupt halt bears a cha racter otf a regularity regan:ioless of the age of formation (cf. Sturani 1971; Wendt 19171; ScholI & Wendt 1971; Krystyn, Schiiffer & Schlager 1971). The neptunian dykes oonnected with the capreef in the DevOOlian of the Rhine Shale Mts {Fran1ke 1971, Krebs 1971) and the Holy Cross Mts (Szu'l czewSki. 1971 and the present paper) extend this regularity to the Devonian. Three iundamentai manners of fissure opening iJn carbonate rocks in prinCiple exhaust the ways of fueicr:- forma:tion ,(Fischer 1964, p. 133). These are: tectonic fracturing, Jarge scale mud-cracking and a karstic solution. The neptunian dykes on the Dalnia Hill are distinctly of tec tonic origin. Their sharp margim and the lack of evidenc-e of karstic so lution confirm tihds fact. The supposed facial position oif their filling also indicates thart the opening and filling of fissures took plaICe under submarine .coruii ,tiorrs. Here, it should be added that the opening and complete filling df fissures was repeated several times and took place in the process otf sedimentation on a submarine ridge. This is indicated by a vertical trace of the boundaries of sediments of various ages which is parallel to the walls of fissure. The opening of the fissure occurred at least tWlO times, that is, iill the Upper Palmatolepis quadrantinodosa Zone .and in the Middle Spathognathodus costatus Zone. It :is ddIficult to say for certain whetiher the fissure was later gradually filleld up to the end of the Gatten'doI'fia Zone or was it seveTa:! times opened and filled, but the former of the two possibilities seems to be more -probable. The reo pendng otf the Famenniaill dykes in 1Jhe Tournalisian closely resemlbles the condi"tioo Which were p,redominantin the lIleptunian dykes in the Gau dembach quarry in the Rhine Shale Mts (Krebs 1971, Ip. 58). Thus, the neptunian dykes at Daln[a correspond. only to fragments of the original condensed sequence. PALEOGEOGRAPHICAL AND PALEOTECTONIC SIGNIFICANCE The determination o!f the age af the neptUIllian dykes throws a new 'light on the stratigraphy and Tecanstructian of the profile at Dalnia. The oolitic limestones which make up the 'bedrock of neptuillian dykes overlie the limestones of the stromatoporoid-corai fades. The thickness of the oolitic limestones amounts to about a ibare 2 m. They we're descrilbed and iUusttrated eat.Li.er (Szulczewski 1971, pp. 63 anJd 106; PI. 2'9, Fig. 1). At first, the views were expressed (Szulczews'ki 1971, p. 63) that the oolitic limestones represeiIlt the entixe FameIllIliaLn. or at Jeast a coosidera'ble, strongly condensed part. This supposition washased on finding in ,an only positive sample of the oolitic limestone a scarce, mixed conodont faU/Ila 30 MICHAl. SZULCZEWSKI indicating to III and to V/VI-VI. Now, however, it has been found beyond any doubt that the dep:osits of to IlIa are situated even in the mssure in filling and, therefore, ·the oolitic limestones have to be as whole older than these deposits. The sample mentioned above contained prObably ce!rtain con'Odonts 'coming not from the oolitic limestone but froOm a small neptunian dyke interesecting it. Thus, the oolitic limestones represent a higher, indetemninate part of the Frasnian or the lowermost Famen nian. In this oonnection there arises a new possibility of interpreting the block of cepha1opod [imestones, which rests at the foot of the Dalnia Hill (Szulczewski 1971, p. 64) and 'Contains conodonts which indicate the Lower or Middle PaJmatolepis 'Crepi~ da Zone (to IIa). Using the ,present stratigraphic inte1'lpretation of the oolitic lime~ stones, it seems likely that the cephaiJ.opod limestones originally occurred on the Dal7rla Hill directly on or, through some so far unknown mellllbers, over the oolitic limestones. Thus, the oolitic limestones would be most likely older than the !.oweI,' Palmatolepiscrepida Zone. No information has hitherto been avai:1able on possibly existing deposits from the Zones between the Lower or Middle Palmatolepis ·crepida Zone and the Upper Palma'tolepis quadrantinodosa Zone on the Dalnia Hill. The .locality {)if the Famennian and Toumaisian on the Dalnia Hill is ·eXlceptional in the Holy Cross Mts and its presence results in several cOIllsequences of a regdona'l importance. . The condensed prOifHes od: the entire Famennian have so far 'been knoWtn in the western part of the Holy Cross Mts only from the southern part Off this area, primari,ly from Gal~ce (Czarnooki 1928). Excluding the a'lmost entire Cheiloceras Zone (cf. Wolska 1967), the Famen:nianof that locality is only 3 to 4 m i!l1 thi,cmess. The character of a condensed sequence ds also dbselrved in the Fant.ennian of Jablonna (cf. Wolska 1967); . . . . whioh is about 8 m 'thick, Less condensed is the FamenniatIl profile iI\ the Bolechowice borehole 1 (cf. Za'kowa 1967, Freyer & Za'kowa 1967), where the deposits from the Upper Palmatolepis crepida Zone (not thE'! Lower P. crep,ida Zone as regarded by Freyer & Zakowa 19'67) up to thE'! end of the Devonian are about 25 ID 1hlcik. All the localities mentioned above are, however, situated on the soufuern side of the Dym1ny antic1inE1; whi'le Dalnia, as an on.'ly loca:lity of this type, is sitwated 0Ill the norther~ s'ide some 9 km :from a strip of so far known localities with the condelJ.:; sed Famennian. Between' them and Dalnia, the Famennian deposits arE'! eroded in the 'core ,QIf the Dyminyantioline and its eastern tectonic equi": valents. Outside of this area, that is, in 1Jhe north (Czarnow - Kielce ~-. ~ Zagorze - Radlin) ami in the west (Daleszyce - Kowala - Wola ~u:- fowana) , the FaJInennian is deveLoped in the !basin facies (cf. Szulc~~w- ski 1971) and is 100 to 200 m 1ihick. Ln the 3OIUth-west, the Imowl~- o( the Famenruian is strOOlgly fragmentary and in the west the Pa1eo~~ ae~ ; posits are hidden tilnder the Petrmian-iMesozoic formatiiOns (cJ.'~ig; - 1).' ,I. ~ • .~. _ . NElPTUNIAN DYKES AND THEIR CONlODONT FAUNA FROM DALNIA 31 A1though our lrnowledge of the Famennian is for .objective reasons frag mentary, it S€ems likely that the area cor:responding to present-day Dy miny anticline, as well as to the central and eastern part of its southern neighboT, that is, the Gal~zi'Ce-Bolechawi.ce syncline, made up in the Fa mennian a submarin·e rise, on which the 'conditiOttls predomilnated of a low !rate of depositiOlll whiCh led to the formation of condensed sequen ces. At the same time, this area coinddes with the sedimentation area of the stromatopol"Oild-ooral1imestones ,in the Frasnian. This fades was bor dered in the Frasnian, the same as in the Famennian, with deposits' of deeper fames which outcrop (cf. Fig. 1) not only in the north-east (Slu chowic.e - G6rno), but also in the south-east (at Kowala) and in the south -west (the chain otf Mt. Zamkowa at Ch~y). It was a.lJready Czarnocki who suspected the area of the Dyminy anticline as a hypothetical zone of the development of the Framrlan reefs. The overlaJppin'g of the plan of facies in the F,rasnian and Famen1llian here indicates the connection of the zone of the slowed-down Famennian sedimentation to an area which was occupied in the Frasnian iby the reef complex. A relatively fast sedimen tation which toOk rplace in the Famemlianoutside of this area tended to equal the relief inherited Y'€t from the conditions which predominated in the Frasnian. Similar connections of heterochronous facies were suggested in the Rhine Region Iby P.aproth & Streel (1970, p. 389) and Krebs (1971. p. 55) . . The conditions dbserved on the DaInia Hill indicate that the sedi mentation oIf condensed deposits loca11y included not only the Famennian but also might include the entire Toumaisian Gattendorfia Zone. The Tournaisian on the DaInia Hill is unique in ·character in the Holy Cross Mts. It is manifested in an extreme reduction of thidmess, development in the fades ami abundance of f·ossils. In its a'bundance of the fine Cya thaxonia fauna of solitary 'rugose cora1s, trilobites and conodonts, it deci dedly differs from all so far known types of the development of the Lower Carboniferous. In its assemblage of fossils and in lithology, the Tour nalis.ian oIf Da1nia does not resemble at all the Carboniferous limestone of the Visean at Gal~zice and, on 'the other hand, is distinctly related to the type of sedimentation and assemblage of fossils characteristic of con densed sequences in the Famennian. It distinctly stands in contrast with a common development of the Holy Cross Tournaisian which nearly everywhere is developed iIn the Culmian fades of clayey shales 100 to 250 m thick (ZakOiWa 1970). The Bolechowice 1 borehole in which the de posits df this age (F1reyer & Zakowa lS67) are c. 5 m thick is the only locality where the Gattendorfia ZOIIle .is developed also as cOIIlden.sed ca'lcareous-marly formations. However, dating the Carboniferous in this borehole is !rather prolbleanatic since the few .specimens of Siphonodella found there have illot Ibeen deso:ribed or illustrated and species to wmch . they were assi~ed happen to be V'a.ti.ously ilnterpreted. Nevertheless, it MICHA:t. SZULCZEWSKl should be mentioned that ,both localillies with the condensed Tournaisian (Dalnia aTlld Bolechowi'Ce) are situated ·in an area d·eterrnined as a zone ()f the oondensed Famerunian. We should also dwell an the sulbject of the charader of a boundary between the facies of the Famennian-Tournaisian sulbmarine rise and the basin fades which borders it (cf. Fig. 5). 'The tTansibiOil1from the former to the lattar seems to be in .the environs of Dalnia unusually abrupt. At the foot of 't'his hill, between Dalm.ia and Karcz6w'ka, the Famennian oc curs already in the basin fades (cf. Czamocki 1938, Szulc.zewski 1971). The Famennian developed in thlis fades fills ·the axial zone of the Kielce synC'line and reaches c. 150 to 200 m 'in thiCkness. A radical change in fades occur, !therefore, over a space of some scores ·or at most several hundred meters. The desintegration of the carhonate platform by blook -f'aulbin:g was suggesteld (Szulczewski 1971, Text-fig. 11) to explain such sudden changes :in facies. This early, synsedimentary block tectonics and facial changes ,caused .by it were probably the basis for the general outli ne of the later fold tectonics. This Obviously hypothetic conception requires recalling some facts. In the Fra'sniaIl'l, the axis od: the Kielce syncline makes up a borderline between the northern basin facies ("I:.ysog6ry fades" as termed by Czar nOOki) am the reef complex ("Kielce fades" sensu Czamodki). The Fras nian of the northern and southern limb of this syncline radically d.iffer in character. ILn the southern limb the Frasnian is fmmed mostly by mas sive, non..Jbedded limestones, in the northern limb almost the entire Fras nian is develope!d as thin-bedded limestones ·with marly shales. The Fras ,nian deposits of ,both li'mibs differ, therefore, radically in their mecha nical character. In this respect, only the limestones od: the lower part of to la of the northern limb are an equivalent of the massive Frasnian lime .stones of the s'outhern limb of the Kielce synol!ine. The massive strOlIIla toporoid-coral limestones of the southern limb !Were formed. 'in a shallow- Fig. 5 'Upper Devonian and Lower Carboniferous fades distribution and its consequences ;in the Variscan tectonic movements in the western part of the Holy Cross Mts, between Dalnia and Sluchowi-ce (cf. Text-fig. 1) Successive stages are shown for the time of: a - Frasnian b - Famennian through· the Gattendol'lfia Zone at: the T·ournaisian c - Visean d - Variscan orogeny(llthology marked up to the Recent morphology) ;l shales, 1I pe1it1c and marly limestones, 3 detrital l:imestones, 4 biollthic limestones, S condensed sequence with neptunim dykes NEPl'UNIAN DYKE'S AND THEIR CONODONT FAUNA FROM DALNIA 33 ssw c Sea level b Sea leyel a [":""::13 E..:..::..:..=J 3 34 MICHAt. SZULCZEWSKI -water environment, while the thin'"'bedded formations of the northern limlb weTe deposited in a deeper basin facies. A complete equalization of the differentiated relief of the bottom of the tbasin probably took place in the Pericyclus Zone. Up to that time, a c.70 m thick layer of the thin -bedded Frasnian, c. 150 m thick marly Famennian'a!nd probably also se veral scores of meters of the Culmian were deposited in the northern basin. In the Famennian and in the Gattendarfia Zone, -the increase in deposit in the Dalnia region was extremely reduced. From the beginning of the Pericyclus Zone, an fue substrateof the seddmentary basin in fue p,lace corresponding to the present-day Kielce syncline, the deposits which were not strictly of the same age, but which were varying in age and having radically different mechanical ,characters, adjoined each othe!". To the south, the position of marly and thin-bedded deposits of the Frasnian, Famennian and parts of the Tournaisian was taken by massive limesto nes of the Frasnian and probably also Givetian. It is possible that the trace of this principal and distinct line of facial division predestinated to a certain extent the development of later tectonic forms, that is, the Kiel<:e syncIine and the Dyminy anticline in their rejuvenated shape. A ce!rtain light ~s also thrown by the structural conditions in the sutbstrate of the Culm de~osits on the genesis of the Sluchowice fold (cf. Szulczewski 1971, Text-fig. 2). The Sluchowice fold OT ratheT a complex of folds seems to be a particular case of the tectonics of the Upper De VOIliaJrl deposits of lthe western part of the Holy Cross Mts. The folds of an 'impressive size consideraJbly depart in thelir deve10pment from a usually small advanced and flex,ural tectonics of the Upper Devonian. The southe'rn vergence of these folds is concordant with that O!f large!r anticlinal !Units in the Holy Cross Mts, including the IJysogory anticline (cf. F!i.g. 1). It seems likely that the Sluchowice folds in the northern limb of the K'ielce syncline were formed in a pla'ce where the Frasnian, Famen niap and Tournaisian competent dejpOSits subjected to a pressure from the north encountered a resistance of a rigid block of massive Givetian and FTasni'an limestones cortresponding to the block of the present-day DaLrua Hill. THE CONODONTS The material collected OOmprises about 2,800 sp~imens ofoonodonts be~onging too 11 genera and 56 species and subspecies. The frequency of conodonts in . particular samples is not uniform and varies from several scores to more than 1000 per 'kilog,ram of sample. Although the entire material comes from neptunian dykes and many samples contain mixed conodont faunas Wdth elements from the deposits ranging from the Upper Palmatolepis quadrantinodosa Zone of the Upper NEPTUNl'AN DYKES AND THEIR CONODONT FAUNA FROM iDALNIA 35 Devonian to the Siphonodella crenwata Zone of the Lower Carboniferous, that is, from a considerable stratiJgraphic interval, all eonodonts are si.tmi. larly translucent bmwn in calor and do not display any physical ,evidence of reworking, such as abrasiOIl 'OIl' surtface wear met with in some of the rewO'l"kerd conodon'ts !from mixed faunas (e.g. Krebs 19-64, Klapper 1966, Schumacher 1971). It is a characteristic phenomenon that in sampJes con tainiIllg mixed faunas the youngest elements 'are inferior in nu-miber. A similar state of preservatiOIl' and a la1ck of differences between forms Vatrydng in age and coming from mixed faunas :indicate that their accu!muJoati'On was not the result of a redeposition a'long the bottom, but that it was caused by strattigraphic condensation (cf. LinrdstrOm 1964, pp. 71-73; Schumacher 197'1, 'P. 73). Shifting the each 'conodont bearing depo sit into a fissuxe in the bottom was a sulclden and single occurrence, which obviously did not cause a physical destruction of OOIlodontg. This conclu sion is in a complete oonfOlr'mity With previous ones concerning the facia1 character of 'the deposit from the neptunian dykes on the Dalnia Hill, which was formed under the conditions of a very low rate of sedime:n tation and usually in a low-€iIlergy environment. All the species found are listed [Ill Table 1 which a:lso !presents the'ir frequency in samples. The descriptive, paloontologiool part concerns only 29 species, the decisive majority of which have so far been neve!r descri bed or illustrated from 'the Holy Cross Mts or 'Other regdOlIlS of Poland. These are species -confined to the Tourna'isian 'Or uppermost Dev:anian. Descrihed are also some s~ecies of Spathognathodu8 c08tatu8 Bran,s'OIl cOIlcept of which arouse considerable differences in views. The FamelIl nian oonooonts, a OOITect paleontological l]7eoorrd of which was presented by Wolsika (19167) and which do not cause any significant taxonoonic coo trorversies, have 'not !been here described. Without discussing 'them in the text, such selected ~edies are illustrated (Pt 1) which beyonJd -any doulbt prove the presence Of the Famenn'iancondoot foaUlIlas in the n~tunian dykes at Damia. All the photamicrographs of the conodoo1s (PIs 1-6) have been taken by L. Luszczewska, M. Sc. Genus DINODUS Cooper, 1939 (Type species: Dinodus leptu8 Oooper, 1939) . Dinodus wilsoni Druce, 1969 (Pt 3, Fig. 1'1) - ?1956. Dinodus teptu8 Cooper; Blschoff & ziegler, p. 146, PI. 14, Fig. 4. 1969. . Dtnodus wttsont &po IlIOV.; !Druce, p. 114, PI. 3, Fig. Sa, b. Remarks. - The specimen under study has a broken anterior bar which, in the type material, is -three times -as long as the posterior one. Dilnodus witsoni differs from other species of the genus, oonsistmg of two bars, jn having an upright arran- 36 MICHAZ. SZULCZEWSKI gement of the dentic1es. Dinodus youngquisti Klapper has a similar dentition, but i'he thll"ee bars developed distinguish it well from D. wilsoni and ·other s.pecies of the genus. Occurrence. - The scarce Australian type material oomes from the upper cu I - iower cu lIa, probably from the lower cu Ha zone (Druce 1969, pp. 24, 54), but the r·ange of the genus is restricted only to the Tournais.ian of Europe, the LoWell" MiSSissippian (Kinderhook) of North AmerIca and to its equivalents in Australia. Genus POLYGNATHUS Hinde, 1879 (T~e species: PoZygnathus robustic08tatus Bischoff & Zi-egler, 1957) Po,Zygnathuscommunis communis Branson & Mehl, 19.34 (PI. 3, Figs 1~3) 19341b. Polygnathu8 communis n. BP.; BmlUKm. & Meh1, p. 293, Pl. 24, Figs 1-4. 1957. Po1.ygnathu8 commun48 Bl"8lI8Qtl & Mehl; Bischoff, p. a iLpan], PI. 5, Fdgs 24, 'I!I [non Figs 23, 25, 28 = P. pums purus]. 1959. Polygnathus communis Branson & Mehl bifurcata n. V'ar.; HB8I!, p . .390, .F'l. 411, Figs 11-12. 1961. PolygnathUB communis btfurcata HB8I!; scott & CoWnson, pp. lS0--131, Pl. I, F·ig. 11. 1984. Po1.ygnathus communis Br8lllllOn & Meh1; Budurov & T&chunev, PI. 5, Figs la, b; :la, b; 12, 18. 1965. Po1.ygnathus communi8 Branson & Mehl; Spasov, p. 95, PI. 2, Figs 15, 15a. 1988. Potygnathus pura 8ubptana Vogs; M8JI2lOni, !p. 480 [pari], PL 59, Fig. 12 [non Fig. 1 = P. pums 8ubptanus]. 1968. ' Polygnathu8 pura Voges; MaD2Xlni, pp. 479-480, PI. 60, Fig. 3. 1967. Polygnathu8 communis communis Branson & Mehl; van Boogaert, p. 183, PI. 2, Fig. 37. 196'7. Polygnathu8 communis BraalSOll & Meh1; WOilska, p. 411, PI. 14, Figs 1-4. 1968. Po1.ygnathu8 communis Branson & Mehl; ¥.oImd, p. 505, PI. 89, Figs 12, 13, 18. 1969. Polygnathus communis Branson & Meh1; PLATE 1 1, 2 - Palmatolepis quadrantinodosa marginifera Ziegler; upper views of two hypotypes (IGPlS. 185, 186). 3 - Palmatolepis distorta Branson & Mehl; upper view of hypotype (I GPfS. 187). 4 - Patmatolepis glabra Zepta Zieg1er & Huddle; upper view of hypotype (IOPIS. 188). 5 - Palmatolepis gornioctymeniae MUller; upper View of hypo type (IGP/S. 189). 6 - Pll'lmatolepi.s gracilis gracilis Branson & Mehl; upper-Iater·al view of hypotype (IGPIS. 190). 'la, b - Spathognathodus disparilis (Branson & Mehl); upper and inner lateral view of hypotype (IGP/S. 191) - note one node on the dnner extension and -two nodes on the outer extension. Ba, b - Pseudopotygnathus trigonicus Ziegler; ·upper and lower view of hypotype (IGP/S. 192) displaying bifurcate ridge of nodes and corresponding secondary carina on the inner platform. 9a, b - Polygnathu8 symmetricus Branson; upper-lateral and upper view of hyipOtype (IGP/S. 193). . 10 - Spathognathodus gradatus (Youngquist); lateral view of hypotype (IGPIS. 194). 11 - Polylophodonta pergyrata Holmes; upper view of large hypatype (IGP/S. 194). All photographs are X 36 A CTA GE OLOGICA POLONICA, VOL. 23 M. SZULCZE~SKI , PLo 1 ACTA GEOLOGICA POLONICA, VOL. 23 M. SZtiLCZEWS,KI, PLo 2 NEPrUNTAN DYKES AND THEIR CONlODONT FAUNA FiROM.DALNIA 37 1969b. PotYl1nathu8 communis; Matthew., PI. 51, FIlg. U. 1989. Potygnathus communis Branson &. Mehl; Ollvier1, pp. 59-60, PI. 24, Figs 1-1.1. 1989. Potygnathus communis communis Branson &. Mehl; RexroBld, pp. 33-34, PI. 5, Fd.ga '1-10 [tlynOIlymy given]. 1989. Potygnathus communis communis Branean & Mehl; Rhodes, Austin &. Diruce, pp. ~az.,.,184, Pl. l2, Figs z-6. 1989. Potygnathus communis communis Branson & Mehl; ISch6n1aub, p. 333, PI. I, Figs 11-13. 1989. PotygnathuB communis BTanson & Mehl; Zdegler, PI. S, Figs 7--,l1. 19'10. Potygnathus communis Bl'!IImIOIl & Mehl; AU8tin & Rhodes, in Austi.n &: al., PI. I, Fig. 12a, b. 19'10. Potygnathus communis dentatus Druce; l)["uce, p. 98, PI. 1'1, Fig. 411, b. 1970. PotygnathuB communis communis Br·ansan & Mehl; stoppel, pp. 21~9, PI. 29, Fig. U. 19'10. Potygnathus commUnis bifUrcatus Bass; ThOlDipllOIl & FelloWs, p. 92, PI. 3, Figs 1, 5. Remarks. - Some of the specimens collected are closely comparable with the Australian ones designated by Dru<:e (1969) as Polllgnathus commtunis dentatus. Druce considered a dentkulate platform edge at the extreme anterior end of the platform as diagnoStic of the subspecies. However, the specimens displaying this character fall within the range of variability of the nominate subspecies which displays a great variation in the platform ouU1dne and its edge ornamentation. They OCC'Upy ·a position between specimens with unor!ll'amented platform and those (e.g. Bass 1959,Pl 49, Fig. 11; Voges 1959, PI. 34, Fig. 1; Canis 1968, Pl. 72, Fig. 12; Anderson 1969, Pl 109, Figs 13,22) having nodose margins .a'lso in ·the posterior part of the platform. Occurrence. - The emliest occurrence of P. commtunis communis ever recorded is in the Cantabrian Mts where it was found in the Palmatolepis quadrantinodosa Zone (Boogaed 1967, p. 183), but in Germany it was not found (Ziegler 1962, Tab. 5, 6) in deposits older 1!b.an the Lower Polygnathus styriacus Zone (to rv/V). The wide range of the subspecies reaches the Scaliognathus anChoraUs Zone (Voges 1959, Tab. 1) or even cu IIIa ·(Bis·choff 1957, Tab. 2). The range of the subspecies in North. America given by Canis (1968, p. 544) and Anderson (1969, Tab. 1) extends from the Upper Devonian to the Middle Mississippian. For a detailed list of the occurrences of the subspecies - see Olivieri (1969, p. 60). PLATE 2 1,2,5 - Spathognathodus costatus spinuUcoStatus (Bl"anson); upper-lateral views of . ; largehYPQtrpe (IGPIS. 1!)5),andhYPQtype (IGP/S. 196) transitional to S. cos,;. ·tatus J:'Qstatus «Branson); upper viewo:!; hypotype (IGP/S. 199). 3, 4 - Spathognathodus c08tatus costatus (Branson); upper views of two hypotypes (IGP/S; 197, 198). 6- Spathognathodus aculeatus (Branson & Mehl); upper view of hypotype (IGP/S. 200). 7a, b --. Spathognathodus stabilis (Branson & Mehl); lateral and upper views of hypotype (I GP/f:? 201). 8a, b . ~ Protognathod.US meischneri Ziegler; lateral and upper views of hypotype (IGP/S. 202). 9, 10 - Protognathodus collinsoni Ziegler; lateral and upper vi'ewe of hypotype (IGP/S. 203) with incipient ornamentation; upper view of large !hypotype (IGP/S. 2{)4) with broken blade. 11-13 - Protognuthoduskockeli (Bischoff); upper views .of three hypo types (IGP/S. 205, 206, 207) showing differences in the upper surfaceomamentation. Ha, b - Pseudopolllgnathus sp. A.; upper and lower. Views of hY'POtype (IGP/S. 208). All·photographs· are X 36 MICHAl, SZULCZEWSKI Polygnathus. communis carinus Hass, 1959 (PI. 3, Figs 5-6) 1959. Polygnathu8 communis Branson &: Mehl carina Haar n. vu.;. Hass, p. 391, PI. n, Figs 8--9 [Footnote 3: "This variety is a su~"]. 1959. Potygnathus communis BraIUJOn &: iMehl VIIIr. carina HaE6; VogeB, pp. 2&lJ-..480 [part], PI. 34, Figs 5--6, 1964. Pol.ygnathus communis carina Hass; ReXll'oad &: Scott, p. 34, PI. 2, Figs .24---{.!5. 1967. Potygnathu8 communis carina Hass; van BOogaer·t,p. 184, PI. 2, Fig. 43. 1967. Potygnathus communis carina Hass; Thompson, pp. 45---46, PI. 2, Figs 7, 10; PI. 4, Flgs 6, 9. 1968. PotygnathuB communis carina HaSB; Can!ls, p. 544, PI. 72, Fi.g:s 18--20. 1968. Potygnathu8 communts var. carina Hass; ManzOIIli, p. 684, PI. 61, Figs a-a. 1969. Potygnathu8 communis carinus Hass; Druce, p. 95, PI. lB, Fig. 12a-c. 1970. Potygnathus communis carinus 'FLaIls; Thompson &: Fellows, pp. 9a-93, ' PI. 3, FJg. 14. Remarks.- Polygnathus communis carinus differs from the nominate sub species in having nodose ridges in the an-terior part of the upper su1'face.' Specimens transItional to Polygnathus vogesi frequently occur in the material], 'collected. For a comparison lWi,th P. 'Vogesi -'- see Voges (1959, p. 294). . Occurrence. - According to IVoges {1959, pp. 27, 209), Polygnathus communis carinU80CCurs in Sauedand from the Protognathodus lrockeli - Pseudopolygnathus dentiiineatus Zone '(CU 1) to the Scaliognathus anchoralis Zone (cu IIP/y). Rexroad & Scott (1964, p. 15) and ThOInPSOO (1967, p. 46) record this substpecies in North America from the Gnathodus semi~alber Zone to the Pseudopolygnathus multistriatus Zone. It was 'also Ifound :in Australia, probably in the lower cu IIa Zone (Druce 1969, p.24). Polygnathus cif. flabellus Branson & Mehl, 1938 (Pl. 3, Fig. lOa-b) ct. 1938. PolygnathuB ;ftabeUa n. Bp.; Branson &: Mehl, p. 147, PI. 34, Fig. ~., 1968. POI.ygnathus ftabeUa (Bra.D8OIl &: Mehl); p. 685 tpanJ, PI. 62, Fig. 17 [OIIlly]. PLATE 3 1-3 . - Polygnathus communts communis BTanson & Mehl; upper view of hypotype (!GP/S. 209), upper-lateral and upper views of hypotype (lGP/S. 210), upper view of hypoty,pe (l,GPIS. 211). 4 - Polygnathus oogesi Ziegler; upper view of hypotype (lGP/S. 212). 5, 6 --j Polygnathus communis carinus Hass; upper view of hypotype (lGP/S. 213), upper and 10lWel' views of hypotype (lGP/S. 214). 7 - Polygnathus purns purus Voges; upper view of hypotype (lGP/S. 215). 8 - Polygnathus inorrnatus Branson; upper view of hypotype (lGP/S. 216). 9 - Polygnathus purus subplanus Voges; upper view of hypotype (lGP/S. 217). lOa, b - PoZygnathus cf. flabellus Bransan & Mehl; lower and upper views of hypo type (lGP/S. 2.18) with broken Made. .11 - Dinodus wilsoni Druce; outer lateral view of hypo type {lGP/S. 219). 12, 14, 15 - Polygnathus symmetricus Branson; 'upper and lower views of hypotype (lGP/S. 220),upper views of two hypotypes (!GP/S. 222, 223). 13- Polygnathus longiposticus Branson & Mehl;upper view of hypo type (lGP/S. 221). All photographs are X 36 ACTA GEOLOGICA POLONICA, VOL. 23 M. SZULCZEWSKI, PL. 3 ACTA GEOlJOGICA POLONicA, vol.. 23 M. SZULCZJ;;WSKi. ,pL o 4 NEPTUNTAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 39 Remarks. - The only specimen available displays a wide, nearly cireular platform rw.ith 'a gently rounded posterior margin. The upper surfaee ornamented with radial, naTrow ridges. Carina separated from the anterior pm-t of platform by deep troughs. Anterior parts of pla'tform are O1'namented between the troughs and ma;rgin of platform with a few nodes and not ridges. Carina does not !['each the 'posterior end of platform. In having more circular pila'tform and partly nodose ornamentation the specimen in hand differs f!['om the holotype. Occurrence. - The holotype ,of Branson & Mehl (1938) comes from the Lower Mis'sissippian of Missouri, ibut the specimen in hand concurs with the eonodont as semblage diagnostic for Palmatolepis quadrantinodosa Zone. Polygnathus inornatus Branson, 1934 (PI. 3, Fig. 8) 1934b. Potygnathus inornata n. sp.; Bn,nson, p. 309, PI. 25, Figs 8, 26, [Fig. 8 = lectotype selected by Klapper, 1971]. 1966. Potygnathus inornata Branson; Klapper, pp. 19-20, PI. 1, Figs 9, 10, 13, 14 [only; synonymy to 1966 given]. 1967. Potygnathu8 inornata Branson; van Boogaert, p. 184, PI. 2, Figs 39-40. 1969. Potygnathu8 tnornata Brans>Olll; SCh6nlaub, p. 335, PI. 1, Fdgs 18-19. 1970. Potygnathu8 ignoratu8 [sic] Bra,nson & Melhl; Austdn & Rexroad, in AUBbin & al., PI. 1, Fdgs 15, 19. 1971. Potygnathu8 inornatu8 Branson; K~per, NI. 6-7 [synonymy gdven]. Remarks. - As pointed out by Klapper (1971, !p. 7), there is no coincidence in the concept of PoLygnathus inornatus in BTanson (1934) and B!['anson & Mehl (1934) and tWIO separate species were sometimes deseribed under that name. E. R. Branson is considered to be the author o.f P. VnornatUs and, eonsequently, P. inornatus sensu Branson & Mehl is temporari[y [eft without a name. The 'concept of P. inornatus is . here !['estrlcted to P. inornatus sensu Branson. According to Klapper (L. c.), P. inor natus Branson has an asymmetrical platform alDd characteristically sinuous posterior carina, whereas P. inornatus sensu Branson & Mehl has a straight blade alDd carina, its platform being almost symmetrical. For the :reasons also given by Klapper (1971) P. Zobatus is here iooClluded in P. inornatus. Occurrence. - According to Klapper (1966, p. 20), the :range of P. inornatus, which a.bio indudes forms now regarded as P. inornatus sensu Branson & Mehl, ext€nds ,from to V s'trata {Bischaff & Ziegler 1956) to the Scaliognathus anchoraUs Zone (Voges 1959) lOT cu IlIa (Bischoff 1957). PLATE 4 la-c - PseudopoLygnathus sp. B; lateral, upper and lower views of hypotype (IGP/S. 224). 2-4 --t PseudopoZygnathus nooomarginatus (Branson); upper views of two hypo types (IGP/S. 225, 226); lower and upper views of hypo type (IGP/S. 22'1). 5-8 - PseudopoZygnathus primus Branson & Mehl; lower and upper views of hypotype (I GP/S. 228), upper and lower views of hypotype(IGP/S. 229), upper view of hypotype (IGP/S. 230), lower and upper views of hypo type (IGPIS. 231). 9a, b - PoZygnathussymmetricus Branson; 'upper and lower views of hypotype (IGP/S. 232). All photographs are X 36 40 MICHAt. SZULCZEWSKI Polygnathus longiposticus Branson & Mehl, 1934 (PI. 3, Fig. 13) 193tb. Polygnathus longilposttca n. sp.; Branson & Mehl, p. 2114, Pl. 24, Figs 8-11, 13. 1966. Polygnathus longtpoBttca Branson & Mehl; Klapper, pp. 2()-'.IJ., PI. 4, Figs 1, 5 [synonymy given]. 1968. Polygnathus longtpo8ttca Branson & Mehl; Ca,nds, p. 545, PI. 72, Fig. 26. 1968. Potygnathus longtposttca BNllDBOID. & Mehl; straka, p. 32, PI. 1, Figs 1~, 10, 14, 15, 18; PI. 2, Fdgs 1~, 6,7. 1969. POlygnathu8 lon.gtpo8ttcus Branson & Mehlj' Anderaon, p. 923, PI. 107, Figs 1, 5, 8, 12. 1969. Potygnathus tongip08ttcU8Branson & Mehl; ReXl'oad, pp. ~6, PI. 5, Figs 11-12. 1970. POlygnathus tobatus Branson & Mehl; Austin & Reuoad, in Austin c!l: at., PI. 1, Fig. lI2a, b. Remarks. - Differences between PoZygnathus Zongiposticus and P. inornatus were listed by Branson & Mehl (1934, p. 293)., Klapper (1966) considers the degree of upturning of the anterolateral margins of the platform as the main ones. Accordingly P. Zongiposticus has its anterolateral margins upturned about to the level of carina. Prominent denticles at the posterior end of the carina are also characteristic of the speci'es. Occurrence. - According to Rexroad (1964), this species is restricted to the Lower Mississippian (Kinderhookian) of North Ameri'ca. Canis (1968, Tab. 2) records its range from the Gnathodus sp. B (= Protognathodus kuehni Ziegler & Leuteritz) - Protognathodus kockeli Zone to the SiphOlIlodella quadruplicata - S. crenulata Zone of Missouri. P. longiposticus has not been reported from Eill"ope. Polygnathus purus purus Voges, 1959 (PI. 3, Fig. 7) 1939. Potygnathu8 marginata Bl'anson & Mehl; Cooper, p. 401, PL 41, Fdgs 11>-16. 1957. :Potygnathus communis Branson & Mehl; 'BIachQff, p. 42 [part], PI. 5, Figs 23, 25, 26 [non Figs 24, 27 = P. communis communis]. 1959~ Potygnathus pura pura n. subsp.; Voges, pp. 291-492, PI. 34, Figs 21--.26. [non] 1966. POlygnathus pUTa pura Voges; Manzoni, pp. 4711--480, PI. 60, Fig. 3 [= P. communis communis]. 1967. Potygnathus pura pura Voges; SpaBOV & Filipovi6, p. 75, PI. 6, Figs 1, 2, 11, 12. 1968. Potygna.thus pura pura vogea; MmIIron1, p. 668, PI. 82, Fdgs 1>-6. ·1989. Potygnathus PUT'US PUT'US Voges; Oliviel"ii, pp. 67-68, PL 11, Figs 9-11; PI. 25, figs 1---3. 1969. potygnathus pura pura Voges; Sch6nJ.aub, p. 338, PI. 1, Fig. 16. Remarks. - The nominate S'Uibspecies of PoZygnathus purus displays a nearly flat, asymmetrical platform. Its Uipper surface is unornamented. The specimens collected conform with ,the origina!l. diagnosis 'and description of Voges (1959). PLATE 5 1,7-9 - Pseudopolygnathus triarnguZus pinnatus Voges; lower and upper views of hypotype (IGP/S. 233) with broOken iblade,upper view of hypotype (!GP/S. 239), upper and [ower views of two hypotypes (IGP/S. 240, 241). 2, 4 - Pseudopolygnathus fusiformis Branson & Mehl; lateral, lower and upper' views of large bypotype (IGP/S. 234), upper and lower views of small hypo:" type (IGP/S. 236). :ta, b - PseudopoZygnathus marginatus (Branson & Mehl); upper and lower views of hypotype (!GP/S. 235). 5, 6 - PseudopolYonathus dentiZineatus Branson;upper views of two' hypotypes (IGPIS. 237, 238). All photographs are X :t6 ACT A GEOLOGICA P OLONICA, VOL. a3 M. SZULCzE'WSkf, 1'1... ~ ACTA GiWLOGICA POLONICA, VOL. 2.3 M . SZ'OLCZEWSKI, PL. 6 NEPTUNIAN DYKES AND THEIR CONODONT FAUNA FROM DA'LNIA 41 Occurrence. - Voges (1959, Tab. 1) records the range of the subspecies in Sauerland from the upper pa,rt of the P,rotognathodus kockeIi - Pseudopolygnathus. dentiolineatus Zone to the top of the Siphonodella - ,triangulus triangulus Zone, but the subspecies ranges as high as Siphonodella ~renulata Zone in the Carnic Alps (Schonlaub 1969, Tab. 1). Polygnathus purus subplanus Voges, 1959 (RI. 3, Fig. 9) 1959. po!ygnathus pura subp!ana n. Sp., Voges, pp. 292-200, Pt 34, Figs 27-33, 1966. Po!ygnathus pura subp!ana Voges; Manzoni, p. 480 [part], Pt 59, Fig, 1 [non FIg. 12 = P. communis communis]. 1968. Po!ygnathus pura subp!ana Voges; Manzon'i, p. 669, Pt 62, Fig. 7. 1969. Po!ygnathus pura subp!ana Vogesi Schonlaub, p . 336, Pt. 62, Fig. 7. Remarks. - The subspecies PoLygnathus purus is characterized by strongly upturned margins 'of the platform, ,pa,rticularly so in its anterior and middle part. The upper surface of the platform is unornamented. For differences with the no minate subspecies and PoLy'gnathus communis - see Voges (1959, p. 293). The spe cimen under study assllgned to this subspecies conforms with the original diagnosis and description of the type material. Voges (Lc.) stated P. purus subpLanus to be the ancestor ,of the nominate subspecies. Occurrence. - Voges (1959, Tab. 1) records the range of P. purus subpLanus from the Protognathodus kockeli - Pseudopolygnathus dentilineatus Zone to the Siphonocielia - triangulus inaequalis Zone in Sauerland. Schonlaub (1969, Tab. 1) confirms such a range of this subspecies in t he Carnic Alps. Polygnathus symmetricus Branson, 1934 {Pl. 1, Fig. 9a~b; PI. 3, Figs 1,2, 14---<15; PI. 4, Fig. 9a-b) 1934. Po!ygnathus symmetrica n. sp.; Branson, p. :UO, Pl. 25, FJg. 11. 1966. Po!ygnathus symmetrica Branson; Klapper, p. 21, Pt 4, Figs 7, 9; Pl. 6, Figs 1, 5 {syno nymy given]. 1966. Po!ygnathus symmetrica Bra,nson; Anderson, Pt 51, Figs 1, 5. 1968. Po!ygnathus symmetrica Branson; ,Stl'aka, p. 35, Pt 1, Figs 6, 9 [non F,igs 11, 13 = P. inor natus sensu Branson & Mehl]. PLATE 6 1, 2 - SiphonodeHa sukata (Huddle); lower and upper views of hypotype (IGP/S. 242), upper view of hypotype (IGP/S . 243). 3-5,8,10 - SiphonodeHa dupLicata (Branson & Mehl); upper views of two small hy potypes (IGP/S. 244, 245), lower and upper views of hypotype (IGP/S. 246} showing a tendency to S. Lobata (Branson & Mehl), upper views of two large hypotypes (!GP/S. 249, 251). 6, 7 - SiphonodeHa quadrupUcata (Branson & Mehl); upper views of two hypo types (!GP/S. 247, 248). i) - SiphomodeHa obsoLeta Hass; lower and upper views of small hypo type (IGPI IS. 250). 11,12 - SiphonodeHa Lobata (Bran'son & Mehl); lower and upper views of hypotype '(lGP/S. 252), upper view of hypotype (IGP/S. 253). All photographs are X 36 42 MICRA!. SZULCZEiWSKI 1969. PotygnathuB symmet7'tcus BraIIBon; Anderson, p. 924, PI. 107, Figs 2, 4, 14, 15 [non Figs 9, 11 = P. tno7'natus sensu Bransoon & Mehl]. 1989. Potygnathus ·antdu8Cooper; Druce, pp. 91-92, PI. 22, Figs 1-4. 11969. Potygnathu8 symmetTtca Bransoon; SchOnlaub, p. 33'1, PI. 1, Fig. 27; PI. 2, Fig. 23. 1970. Potygnathu8 symmet7'tcus BrllillBOIl; Auetin & Rhodes, in Austin & al., PI. 1, Figs 20--21. 1970. Potygnathus Symmetmus Bra,nson; ThIompson & Fellows, p. 97, PI. 4, Figs l7~18. Remarks. - Polygnathus symmetricus is markedly related to P. inornatus and P. longiposticus. Many transitional specimens between P. symmetricus and P. longi posticus (e.g., type material of former P. anida Cooper, P. biclavula Youngquist & Patterson, P. spicata Branson, P. macra Cooper) placed by Klapper (1966) in the synonymy of P. symmetricus, are regarded by other authors as P. longiposticus. The limit here drawn ,between the two species is, however, according to Klapper's (1966) practice as arbitrary as other concepts. Occurrence. - P. symmetricus has been recorded in Europe from to VI strata {Bischoff 1957, Tab. 2), cu I strata {SchOnlaub 1969, Tab. 1; Austin & a!. 1970, Fig. 2) and cu II strata (Bischoff & Ziegler 1956). Polygnathu8 vogesi Ziegle:r, 1962 (PI. 3, Firg. 4) 1962. Potygnathu8 vogesi n. sp.; z.iegIer, pp. 94-95, PI. 11, Figs 1>-7 [synonymy given]. f=] 1967. Potygnathus vogesi Ziegler; Spasov & Fi1ipovic, pp. 71>-78, PI. 8, Fig. 3. 1989. Potygnathu8 vogesi ziegler; SchllonLaub, p. 337, PI. 1, F!lg. 10. Remarks. - For diagnosis of Polygrnathus vogesi - see Ziegler (1962, .p. 95). The differences between P. vogesi and P. communis carinus are examined by Voges (1959, p. 294). Occurrence. - P. vogesi occurs in the uppermost part of the Upper Devonian and in the lowermost part of the Lower Carboniferous. Ziegler (1962, p. 95) ;records it in the Upper Devonian, begiruJ.ing from the Middle Spathognathodus costatus Zone. Voges (1959, Tab. 1, as Polygnathus cf. styriaca) found it in the Lower Carbo niferous Protognathodus kockeli - Pseudopolygnathus dentilineatllS Zone to the Siphonodella - triangulus ,triangulus Zone. Genus PROTOGNATHODUS Ziegler, 1969 (TypeSlpecies: Gnathodu8 kockeli BischOlff, 1957) Protognathodu8 collinsoni ZiegIer, 1969 I(PI. 2, Figs 9-10) ~9&1. Gnathodu8 cf. commutatuB (Bl'IIIiIIIIOn & Mehl>; 'Scott & Colli.nllOn, p. 123, PI. 1, Figs 23-25 ,{non Fdg/I 28, 27 = P. metschneTt]. :1989. PTotognathodu8 coUlnsoni n. lIP.; Ziegler, pp. 3530--.'154, PI. 1, Fig/l J3-18. Remarks. - Thds species of Protogrnathodus displays a slightly asymmetrical ;platform omamented on the upper surface of its inner or outer part by a few nodes. In its platform outline and ornamentation, P. collinsoni may be placed between P. meischnert and P. kockeli. According to Ziegler (1969, p. 354), P. collinsoni differs .from P. meischneriin halVing an asymmetrical platform whi{!h is rathersymmetricai ;in the latter and in a sIlightly nodose ornamentation being in 'COntrast to an unorna menrted upper 'surface af the platiform in P. meischneri. One af the specimens ill:1u tStrated (PL 2, Fig. 9) displays an only incipient nodose ornamentation on the outer ~ide of the platform but a definitely asymmetrical platform outline is characteristic .of the species. NE.PTUNrAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA .43 P. collimsani is morl?hologically nearly 1dentical with Gnathodus commutatus nodosus, but the two species are considered as homeomorphs for the same reasons as those in P. meischneri and Gnathodu8 commutOJtus commutatus. Occurrence. - Ziegler & Leuteritz, in Koch and Leuteritz & Zi~er (1970, Tab. 2), record P. coUinsoni in Seiler from the interval with the "ITotognathodus -Fauna", as well as from the Siph'Onodella sulcata - Protognathodus kockeli Zone. Protognathodu8 meischneri Ziegler, 1969 (Pl. 2, Fig. 8a-b) 1961. GnathoduB cf. commutatuB (Branson & Mehl); Soott & Colltn5on, p. 123, PI. 1, FLgs 26--27 '[only]. 1962. Gnathodu8 n. Sip. A; CollinBo.n, Scatt & Rexroad, pp. 18--19, Char.t 3. 1964. Gnathodu8 Sip. A; Hlgglins, in Hil.ggi.na, Wagner-Gemls & Wagner, p . 22'1, PI. 5, Fig. 28 • . 1967. Gnathodus Sip. A Col1imKm, Scott & Rexroad;VI8.n Boogaert, p. 180, PI. 2, Fig. 22. 1968. Gnathodus lIP. A Collinson,Sootlt & Rexroad; Canis, p. 1i39, PI. 74, Fig. 11. 1969. Gnathodu8 n. SIP.; Rexroad, pp. 19-20 .[part], PI. 4, Fig. 2 {only]. 1969. Protogna.thodu8 metschnert n. SIP.; Ziegler, p. 353, PI. 1, Fig!! 1--.13. Remarks. - A nearlly symmetrical unornamented platform characterizes this species of Protognathodus. MorphologkaMy it is nearily identieal with Gnathodu8 commutatus commutatus Branson & Mehl, but the two homeomorph species, as well as oolTesponding genera Me separated by a ()Ol)Sidera:ble gap, since Protognathodus meischneTi occurs in the lower part of the Toumaisian, whlle Gnathodus commutatus commutatus is not known in beds older than Visean. Aecoroing to .Rexroad (1969), the main difference between the two species is in the shape of denticles on the car ina which are e~icaQ, their greatest dimension being transverse .to the axis of G. commutatus as 'Opposed to the laterally compressed denticles of the forms now as signed to Protogrnathodus meischneri and P. collinsoni. Sueh forms have been con sidered (but unnamed) by Rexroad (1969) as a species pl'obably divided into four subspecies. One of them is exactly compaa.-able with P. meischneri. The specimen illustrated displays a similarity to P. colLinsoniin its slightly asymmetrical platform outline. Occurrence. - Zieg'ler & Leutedtz, in Koch, Leuteritz & Ziegler (1970, Tab. 2), record P. meischneri in the Sei11.er from the interval with ''Protognathodus-Fauna'' and from .the lower part of the SiphonodeMa - triangulus inaequalis Zone. Protognathodus kockeli (Bischoff, 1957) . {PI. '2, Figs 11-13) 195'1. GnathOdu8 kockett n.8p.; Bdschoff, p. 25, PI. 3, FigII 27---U. 1964. Gnathodu8 kocketi iBlscboff; Higgilna, in HdggiDll, Wagner-Gentds & Wagner, PI. 5, Fig. 27. 196'1. Gnathodu8 kockett Blschoff; van BoOgaert, p. 179, PI. 2, Figs 17-18. . 1968. Gnathodu8 kocketi Bischoff; Can!is, p. 538, PI. 74, FiLgs 12, 22; 1968. Gnathodu8 kockeU Blschoff; :Ma1lZi)ni, pp. 659-660, PI. 62, Figs 2, 4. 1969. Gnathodu8 n. ~.; Rexroad, pp. 19-40 .[part], PI. f, Figs 4t-7 [only]. 1969. Gnathodus kockeU Bischoff; Sch6nlaub, ,po 330, PI. 1, Figs 1-2. 1970. Protognathodu8 kockeU (Blschoff); Ziegler & Leuteritz, in KOCh, Le.tite.ritz & Ziegler, Pl. 8, Figs 1-3, 5. Remark'S. - Ziegler (1969) included this species, previously assigned to the genus Gnathodus, in the new genus Protognathodus which is a homeomorph of the former. The two genera are separated by a ·considerable gap. For remarks 'on the 44 MlCHAl. SZULCZEWSKI vadabiUty of PTotognathoous kockeZi and differell'ces between it and P. coZZinsoni - see Ziegler (1969, pp. 354--355). Occ'UTTefIlCe. - Zieg'ler & Leuteritz, in Koch; Leuteritz & Ziegler (1970, Tab. 2), !record the species in 1Jb.e Seiler from the inta-va'l with "Protognathodus-Fauna" to Siphonode'lll.a - triangulus triangru1us Zone. other European occurrences fall within the range of the species. In NOil"th America, PTotognathod'Us kockeli occurs in the Louisiana Limestone in a position corresponding to the interval with "Protognath,o dus-Fauna" of Germany (Soott & Collinson 1961, Klapper & al. 1971) ,and ID the Hannibal Shale (c'U I) in Missouri (Canis 1968, p. 538). Genus PSEUDOPOLYGNATHUS Bran-son & MeM, 1934 '(Type species: PseudopolygnaVhus primus Branson & MOOI, 1934) Pseudopolygnathus dentilineatus Branson, 1934 (PI. 5, Figs 5-6) 1934. Pseudopotygnathus dentittneata n. sp.: BraJIllSOll, p. 317, PI. 26, Fig. 23. 1966. Pseudopotygnathu8 denttnneata Bra,nson: Klapper, pp. 14-45, PI. 5, Figs 10--11 {synony- my gI!.ven]. 1967. Pseudopotygnathus denttttneata Bramscxn: van Boogaert, p. 185, Pl. 3, Fig. 8. 1967. Pseudopolygnathu8 d.entUtneata iSrai!lSOn: Spasov & Fllipovi6, $I. 77, !Pl. 5, Figs 4, 6, 9. 1968. Pseudopotygnathus denttuneata 'Bx6nsan.: 'Canis, p. 546 o[pairt] , PI. 73, Figs 10, 29 [Inon Fdgs 30, 31 = P. prtmus]. 1968. . Pseudopotygnathu8 dentUtneata BraJDSOn: MaIwonl, p. 670, PI. 61, Figs 11, 18, 19. 1969. Pseudopotygna,thu8 dentUtneatus BramlOn; Ollvierl, pp. '1'3-'14, PI. 24, Fig. 7a--c. 1969. Pseudopotygnathu8 denttttneatus BraJlSOll; Rexroad, p. 38, PI. 4, Figs 11----10. 1969. Pseudopotygnathus denttttneatus Brall8Oll; Rhodes, Austin & Druce, pp. 2011----209, PI. 5, . Fd,gs 10, 12, .J.3; PI. 8, Fig: 8 'Dnon PI. 5, FiIg. 9 = dndet. juv. specimen of Spathognathodus or Pseudopotygnathu8 (1); non Fig. 11 = Spathognathodus Bp. indet]. 1969. pseudopotygnathus expan8U8 ~. nov.; Rhodes, Austin & Druce, pp. 209-210, PI. 5, Figs ~ ~ . 1969. Pseudopotygnathu8 "oges' sp. nov.; Bhodes, Austin & iDruce. pp. 2iS-4l.'1, PI. 5, Figs I, 3, ~ . . 1969. Pseudopotygnathu8 denttttneata Br>a!llSOI1; SchO~1aub, p. 338, PI. 3, FIigs 30-31. 19'10. pseudopolygnathu8 denttUneatu8 Branson; Austin & RhodeS, in Austin & aJ,., PI. 1, Figs I, 5, 11\, 14. 1970; Pseudopolygnathus "ogest ReXll"oad,Austln & Diruce; .AustiIJ. & Rhodes, in AllIftin cl al., PL l,Fig. lBa..,..l!._ 1970. Pseudopolygnathu8 denttttneutu8 Bra!nson; Thom~ _& . F~IJQws, p . 99, PI. 5, Figs 1, 5. Remark3. - FOil" differences between Pseudopolygnathus dentiZineatus and P. primus - see remarks on the [atter species. P. dentiZineat'U8 was reooxded fOrmerly not higher than at the top of the Gattendorifia Zone{cu I) ,until Rexroad, Austin & Druce (1969) found specimens nea!1"ly identical with Branson's holotype of P. dentiZineatus also in Avonian conodont zones correlatable with cv. IIP-r. Because of a g'ap between them, Rhodes, Austin & Druce (l.c.) l"Iegarded the spec:imensfrom C'U I and the younger Avonian form from c'UIIP-r -as two discrete and homooIDOrlPhic species. They oonsi-dered the younger one as P. dentiZineatus and the older, including with reservation some ferms fO!l" merly described from Sauel"llanli, as failling into the newly created species P. vogesi. Austin & Rhodes {in Austin & al., 1970) found, however, specimens of both species together in the Etroeungt limestones of Hoyoux va1ley. If the ranges 'Of the two spe cies, !rega['ded as disC!l"ete only on the basis 'Of their unoverlapping tanges, in fact oveTlap 'a considel'aible interval I do not see 'any reason for regarding P. vogesi as a . distinct species. Morphologically, there are no remarkable differences between p~ . dentiZineatus and P. vogesi, wMch woU[d alJlow one to !regard the latte!l" as a dis:.. tind species. Nl!lPTU'NI'AN DYKES AND TH.E::IR CQN1()DONT FAUNA FROM DALNIA 45 Occurrence. - The range of P. dentitineatus extends from the Polygnathus styrlacus Zone to the top of the Gattendorfia Zone in Germany (Ziegler 1962, p. 92). The species was recorded in the Avonian {Rhodes, Austin & Druce 1969) from the Patrognathus var~bilis - Sipathognathodus plumulus Zone to the Siphonodella - Polygnathus inornatus Zone (designated as P. vogesi) and, after a gap, from the Spathognathodus "costatus costatus" Zone to the Gnathodus deUcatus Zone. Sand berg & Klapper (19t17) !l."eoord this species from the Siphonodella sulcata Zone and Siphonode'l!lasandbergi - S. duplicata Zone in Wyoming. CoLlinson, Rexroad & Thompson (1971, F~g. 5) record the range of the species from the Upper Devonian to the top of the Kinderhookian. Pseudopolygnathus fusifcrrmis Branson & Mehl, 1934 (Pl. 5, Figs 2, 4) 19134b. Pseudopol1lgnathu8 fUstformts 10. ~.; BralJlllall & Mehl, p. 298, PI. 23, Figs 1-3. [non] 1966. PBeudopol1lgnathuB fUsiformts Bransan & Mehl; Manzoni, p. 481, Pt 60, Flgs 4-5. 1987. P8eudopot1lgnathu8 fUstfarmt8 BrllllSOl!1 & Mehl; ,"an Boogaert, p. 165, PI. 3, Fig. 7. 1969. pseudopot1lgnathu8 fustfoTmis iBranson & Mehl; Rex·road, pp. 3~, Pt 4, Figs 15-<19 [synonymy given]. 1969. Pseudopot1lgnathu8 fUstfarmi8 Bra.nson & Mehl; SchOnlaub, p. 339, PI. I, Fig. 14. 1970. PBeudopof,1Ignathu8 fustfoTmi8 Branson & lMehl; Thompson & FellJOlws, pp. 99--100, PI. 5, Figs 10, 12, 14- Remarks. - The specimens available a·ocurately correspond to the diagnosis given by Rexil'oad & 500tt (1964, p. 39). According to these authors, PseudopoZygna thus fusiformis gave rise to P. itha (Cooper) [= P. aZZocatus (Cooper)]. According to Rexroad & 5oott, the platform sharply taper~ng posteriorly and the distinctly diffe!l."entiated free blade serve to distinguished P. fusi;formis from P. aZZooatus. In the present material, predominant forms are small. and have a very nar row platform and undistinct omamentatiDn. Occurrence. - Voges (1959) records this species in Sauerland :from the Sipho nodella - triangulus inaequalis Zone and Siphonodelia - triangulus triangulus Zone, but in the Carnic Alps it is also known (SchtinJ.aub, 1969, Tab. 1) from the up per part of the P.rotognathodus kockeli - Pseudopolygnathus dentilineatus Zone. In North America, Ca'nis (1968, Tab. 3) described P. fusiformis from the Siphonodel la sulcata Zone to the lowe!l." part of the Siphonodella quadruplicata - S.orenulata Zone of Missouri. Rexroad & Scott (1964, Tab. 2) do not record it higher than the Siphonodella isosticha - S. cooperi Zone of Indiana. . Pseudopolygnathu8 marginatus (Branson & Mehl, 1934) (PI. 5, Fig.3a-b) 1934b. Pot1lgnathu8 maTgtnata n. sp.; Branson & Mehl, pp. 294-295, PI. 23; Figs ~27. 1968. . Pseudopo11lgnathu8 tTtangma tnaequaUB Voges; :Ma.!moni, pp. 669--6'10, PI. 61, Fig. 7 ,[only]. 1969. pseudopotygnathu8 maTginatuB (BrlllIlBOD. & Mehl); Rex~d, p. 39, Pl. 4, Figs 11-13 [syno nymy given] • .[nan] 1989. Pseudopol11gnathuB maTgtnata (Bransan & Mehl); Sch6nlaub, pp. 339-340, PI. 2, Ftg. 24. 1970. P8eudopol1lgnathuB maTginatUB (Br1l!llllOD. & Mehl); Thompson & FellOW's, Po lOO, PI. 5, Figs 11, 13, 17. Remarks. - A lac'hrimifonn outline of the platform, its upper surface oma mented with transVe!l."Se ridges and 'basal caVlity with characteristic sinus in its flared margins (cf. K!l.apper 1966, p. 13) me among the main characters of this species. The 46 MICHA!. SZULCZEWSKI specimens available display all the charoters. Its platform is reaching the posterior . end of the unit. Occurrence. - Canis (1968, Tab. 3) records P. marginatus feam the Siphonodella su(lcata Zone to the Siphooodella quadruplicata - S. crenulata Zone of Missouri, but ReMoad & Soott (1964, Tab. 2) found is in the Siphonodella isosticha - S. cooped of Indiana. Pseudopolygnathus nooomarginatus (Branson, 1934) (RI. 4, Figs 2-4) 1934. PotygnathuB nodomaTgtnata .n. ap.; BranIsan, p. 310, PI. 25, Fig. 10. 1969. PotygnathuB nodomargtnatusBransan; Oliivderi, pp. 6t--«;, PI. 23, Fig. 8a-b [synonymy given]. 1969. PseudopotygnathuB nodomargtnatus (Branson); Rhodes, Austin & Druce, pp. ~12-213. PI. 9, F'ig3 1-4; Pl. 111, Figs 6-8, 10. 1969. PBeudopotygnathus nodomargtnatus (Branson); Druce, p. 113, PI. 35, Fil!lS 1--3. Lnon] 19'10. PBeudopotygnathuB nodomargtnatus (Branson & Mehl); Austin & Rhodes, in Austin & at, PI. I, Fig. 18. Remarks. - According to the original description of the species given by Bran son (1934, p. 310), each plailform of P. nodomarginatus is ornamented with li'oout seven large ridges not reaching the carina and terminating as rounded nodes on the margins of !platforms. The present specimens display this very type of ornamentatioo, but they are relatively longer and have more nodes (up to 11), much the same as the material presented by some· authors (Olivieri 196'9; Rhodes, Austin & Druce 1969; Druce 1969). The range of variability of the species is not yet satisfactordly establi shed. Most of the previously ilJ.lustrated specimens, placed into the synonymy of P. nodomarginatus by Rhodes, Austin & Druce (1969), are omamenteci with regular ridges and thek platform margins are not nodose. They are not assigned here to P. nodomarginatus. The m.ustration of the holotype in Branson (1934) shows only the upper sur!face of the specimen, but "an exeeptiooally large pit with thick lateral lips" ·00 the lower surface, mentioned in the original description, seems to confirm the assignment of the species by Rhodes, Austin & Dr·uce {1969) to the genus Pseu dopoZygmathus .rather than to PoZygnathus. Specimens described have definitely pseudopolygnathid, large !basal cavity. OccuTrence. - Its lowermost occurrence was found :by 2jiegler (196'2, p. 41) in the Middle Sipathognathadus costatus Zone of Germany. In Great Britai·n, Rhodes, Austin & Druce «1969) give the range of P. nodomarginatus as Upper Zaphrentis (Z) Zone correspOiIlding to the cu IIP-r strata. other occurrences fall IWithin the same range of the species. Pseudopolygnathus primus Branson & Me'hl, 1934 (RI. 4, Figs 5-8) 1934b. PseudopotygnathuB prima n. sp.; BrIlllSOO & Mehl, p. 298, PI. 24, Flg3 24-25. 1966. Pseudopotygnathus prima BI1ansan & Mehl; 'KLa,pper, p. 14, PI. 4, Fig. 8 {synonymy given]. 1988. PseudopotygnathuB prtma Branson lI:Mehl; Canis, p. 547, PI. om, Figs 12, 17, 32. 1988. PBeudopotygnathu8 dentttineata Branson; cands, p. 546 {part], PI. 73, Figs 30--31 .[onlyJ. 1969. PBeudopotygnathuB primuB Bransan & Mehl; Rhodes, Austin & Dr·uce, pp. ~14-2i15, PI. 6, Figs 4, 5, 7, 1&-12. 1969. pseudopotygnathus prtmu8 Bral1180n lI: Mehl; Re:x.road, pp. 39-40, PI. 4, Fig. 14. 1970.. i'seudopotygna.thuB prtmus Branson & iMehl; Thompson & FellOWll, ,pp. llU-.102, PI. 5. Figs 15, 16, 18, 111. NEPTUNIAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 47 Remarks. - An extensive variety of forms formerly described as separate species were included in Pse'UdopoZygnathus pTimus by Klapper (1966) wh.o also drew ,clear distinctions between P. primus and some Il'elated species previous[y grouped !by Voges (1959) in a "group of Pse'UdopoZygnathus primus". According to Voges (1959) and Klapper ,(1966), the main difference between P. primus and P. den tiZiJleatus is in the size of the basal cavity relative ·to the width of the platf.or>m which is larger in the [anter and not covering the entire width of the platform ,aJ; the for mer species. The present material. contains an extensive variety of forms; some of them are illustrated. Forms transitional to P. de-ntiZineatus occur among specimens display ing an aJate interior margin ,of the platform. The last-named are similar to Pseudo poZygnathus trianguZus pinnatus, but as suggested by Klapper (1966), the demarca tion between the two species should be based on the size of basaJ cavity which is smaller :in the latter species. Occurrence. - BischOtff (1957, Tab. 2) records Pse'UdopoZygnathus irreguZaris (= P. primus) in cu I. The species P. primus occupied a !position in the phylogenic lineage between P. dentiZineatus and P. trianguZus trianguZus (Voges 1959, pp. 395- 398, Text-figs 4-5; reinterpreted by Klapper 1966, p. 14) and, therefore, it ·undoubt ly,occurs in Sauerland in beds IIb and IIIa of Voges, whiehcorrespond to the lower part of C'U I, below Siphonodella - triangulus triangulus Zone. Rhodes, Austin & Dr'Uce (1969, p. 2'15) found P. primus in the upper part of the Avonian Spathognat hodus costatus - Gnathodus delioatus Zone 'and in the Polygnathus laC'inatus ZOIne. Sandber Pseudopolygnathus triangulus pinnatus Voges, 1959 (PI. 5, Figs 1, 7-9) 1959. pseudopotygnathu8 trianguta pinnata n. subep.; vages, pp. 302--304, Pt 34, Figs 59--lI8~ PI. 35, FigI! 1-6 [synonymy given]. 1984. Pseudopotygnathus trianguta ptnnata Voge6j HiWns, in HiggIJns, Wagner-Gentis &: Wag ner, PI. 4, Fig. 16. 1964. Pseudopotygnathu8 trianguta vages; ReXil'lOad &: Soott, p. 42, PI. 2, Fig. 28. 1966. Pseudopolygnathus trianguta pinnata Voges; Mamzonl, p. 482, Figs ~ [n:on Fig. 8 P. trtanguta tTianguta]. 1967. Pseudopotygnathus trianguta pinnata Voges; van Boogaert, p. 195, PI. 3, Figs 9-10. 1967. Pseudopotygnathus trianguta VQges; ThOlDlpsoIl, pp. 49-1iO, PI. 4, F'igs 17, 18. 1969. Pseudopotygnathu8 tTiangutus triangutu8 Voges; Druce, p. M4, PI. :r7, wg. 2a-b I[only]. 1969a. Pseudopolygnathus trianguta ptnnata Voges; Matthews, p. 271, PI. 48, Figs 3, 4, 8, 10, 11. 1969b. Pseudopotygnathus triangula pinnata Voges; MattheWB, PI. 51, Fig. 8. 1970. Pseudopotygnathus trtangutu8 pinnatus Voges; Thompson &: Fellows, pp. 102-.103, PI. 6, FIgs 6, 11, 12. Remarks. - This 'Subspecies of Pse'UdopoZygnathus trianguZus is characterized by a strongly alate ·antel'Olateral corner .on the inner side .of its platfoIm. The spe cimens under study differ slightly from the holotype in platform outline, but faU within the range of variability .of the subspecies shoW!Il 'by Voges (1959) and subse quent authors. Some of the 'specimens (e.g. PI. 5, Fig. 9) are similar to P. trianguZus inaequaZis ·in having a J:'ounded outer anterO'later,al >margin and .only indistInctly alate inner anterolateral corner of the platform. It is, h.owever, assigned to P. trian guZus pinrnatus on the basis of a small basal 'cavity, which is relatively large iD P. triangulus inaequaZis. MICRAl. SZULCZEW'SKI Occurrence. - According to Voges {1959, Tab. 1), P. triangulus pinnatus occurs in Sauerland from the Siphonodella crenulata Zone (except for its ilowermost pai"t) to the Sca:liognathus anchoralis Zone, but it is aboundantonly in the latter zone. In CornwalJ1 it was also foun!d by Matthews (1969a) together with a conodont assem blage of the Scaliognathus anchoralis Zone. Collimon, Rexroad & Thompson (1971, Fig. 5) give the !l."ange of the subspecies in the northern Midcontinent of North Ame rica as restricted to the upper part of the Osagean. Pseudopolygnathus sp. A (PI. 2, Fig. 14a-b) Description. - The relatively narrow platform is bisected bya median carina which is continuous with the anteriO!l." and a shO!l."t, posterior free blades. The right side of the platfonn extends farthe!l." anteriorly than does the left. The ornamenta tion differs on the 'two halves of the platform. The entire right side of the platform is om'amented in its posterior ,part with coarse transverse ridges separated by deep troughs and, in the antedor part, with large, transverse, elongate nodes. The poste rior part of the left side bears the same orna.mentation as the right side, but the, anterior part is unornamented. The margin of the right side is chewon-like, much the same a's the posterior part of the margjn of the left side. The margin of the unomamented part of the left side is parallel to carina. In its part corresponding to the unornamented platform carina is composed of completely fused denticles. The anterior free blade consists of laterally ,compressed, fused (except at the tips) 'and gradually decreasing denticles. The posterior free blade consists of small dentides, circular in section. The large basal cavity is situated in the anterior part of platform and it covers the entire width of .the latter. The cavity is asymmetrical, gradually narrowing posteriody and with anterior margins nearly perpendicular to the keel. AgroO'Ve runs along the axis of cavity and extends posteriorly within the keel. Remarks. - These forms retain ,the same type of ornamentation as that of Spathognathodus costatus spinvJicostatus, but differ from the latter in having basal cavity of the polygnathld type, restricted in extent, in contrast to the 'caVity of S. c08tat"Us which is wider than the platform.Pseudopolygnathus sp. A is probably transitional from S. costatus ,to Pset/.dopolygnathus dentilineatus and in the phylo genetic series discussed by Voges (1959, Text-fig. 5) probably falls between the forms from I and 11 beds. The last-named differ from Pseudopolygnathus sp. A only in having the entire upper surface of ,the platform sculptured. Some forms described by Druce (1969, p. 114), as Pseudopolygnathus vogesi are similar to the specimens desCribed, hut differ in having a considerable protrusion on the left margin of the platform, which, in Pseudopolygnathus Sop. A is parallel ,to the carina. Pseudopolygnathussp. B (PI. 4, Fig. la-c) Description. - Platform small, restricted only to the middle part of the unit. A medial, nodose carina is con'tinuous with denticulate anterior and posterior free !bla des. The unit is slightly asymmetrical because the outer platform extends farther an'teriorly than does the inner. The posterior termination of the ,outer platform is also posterior to that of the inner platform. The margins of platform strongly up turned and reaclling the level of carina. Both platforms ol'namented with large trans- NEPTUNIAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 49 verse ridges projecting from a ·crenulate maTgin of platform as chevron-like den tides. The anterior free bla,de is somewhat longer than a half af platfQl"ll1. It con sists of 5 laterally compressed, free-tippe,d denticles; the 3 anterior Qnes are except iooally high. The posterior' free blade is haM the length of the platform and consists (If 5 smaU, laterally compressed denUcles. Basal cavity laTge,covering the entire width .of platform, slightly asymmetri ea1, narrowing rapidly anteriorlyand gradually posteriorly, and dev-eloped in the anterior half of platform. It extends posteriorly as a groove in the keeL' Remarks. - In its outline and ornamentation of the upper sudace Pseudopo lygnathus sp. B is nearly identieal with the forms described by Druce (1969, pp. 105- 106) as Polygnathus toxophorus Cooper. The latter is, however, regarded by Klatpper (1966) as a junior subjective synonym of Polygnathus longiposticus. The basal cavity of the ho1otype of P. toxophorus, actually sman and of the polygnatbid type, stron gly differs from the exceptionally Largepseudopolygnathid type cavity of the speci men under study. Specimens illustrated by Druce (1969) eonsiderably differ in the size of basa!l. cavity, -but n(lne of them displays a cavity as wide as in the specimen described. Genus SIPHONODELLA Branson & Me'hl, 1934 (Type species: Siphonognathus dupUcata Bransan & Mehl, 1934) Siphonodella duplicata (Branson & Mehl, 1934) (PI. 6, Figs 3-5, 8, 10) 1934b. stphonognathus dupttcata n. Bp.; Rransan & Mehl, pp. 296--297, PI. 24, Fdgs 16--17. 1966. StphonodeUa dupttcata (Bransan & Mehl); Klapper, p. 18, PI. 4, Flig. 13 [synonymy given]. {n'OIl] 1966. Sipho.noaeUa dupttcata (BrallllOlll & Mehl); Manzom, p. 484, PI. 60, Figs 1, 2 [Flg. 2 = S. quadrupticata]. 1968. SiphonodeUa dupUcata (Branson & Mehl); canis, pp. 548-549, PI. '12, Fig. 7 .[non Figs 3. 4 = S. quadruplf.cata]. [non] 1966. SltphonodeUa dupltcata (Branson & Mehl); Manzoni, p. 673, PI. 61, Figs 5, 14. 1968. StphonodeUa cf. 8ulcata (Huddle); Main:lloni, pp. 6'l13--674, PI. 61, Flgs 4, ?lOo 1900. S!.phonroella dupUcata (BrllllSaIl & Mehl); Straka, p. 42, PI. 6, Figs 14-15. [non] 1969. SiphonOdeUa duplicata (Branson & Mehl)j ReXll'oad, p. 43, PI.·2, Fig. 13 ,[= S. sut catal. [non} 1969. StphonodeUa dupltcata (Br>anson & Mehl); .schulze, p. 221, PI. 20, Fig. 26 [= s. co opertl. 1969. Stphonodella duplicata (BrB!llSOIl & Mehl); SchOnlaub, pp. 344---1145, IPI. 2, Fligs 9-10. 1970. S!.phonodeUa dupltca·ta (BrlBnson & Mehl); Thampson & FellOwl!,p. 106, PI. 7, Figs 1, 3, 5. Remarks. - The original concept {Branson & Mehl 1934b) of SiphonodeHa du plicata and other siphonooellids wa'S -based on the number ()f rostral ridges. In addi tion to the number 'Of T'Ostral ridges, Bass (1959) and Klapper (1966) oonsidered the taxonomic significance of the ornamentation of platform and restricted the concept of S. duplicata. TrallS'Verse ridges on both sides of platf()rm and tw.o rostra! ridges, usually forming margilllJS 'Of a strong-ly devel'Oped rostrum, are T·egarded after this concept here accepted as the main diagnostic characters of the species. SiphornodeHa duplicata stan·ds closely to S. sulcata and probably al'ose from the latter (cf. Canis 1968, p. '5151). Both s,pecies are omamented by transverse ridges on both sides of the platform but according to Canis (1968), the ridges 'On the inner side of S. duplicata may be composed of 'closely spaced nodes. Acoording to Klapper (1966, p. 18), S. sUl cata differs from S. duplicata in having an only incipiently developed rostrum. On this basis it seems advisable to include to S. suLcata the specimen assigned by Rex road (1969, PI. 2, Fig. 13) to S. duplicata. 4 50 MICHAl. SZULCZEWSKI All specimens in hand have a differentiated ros'from, asymmetrical outline of the platform, small and sli1ilike basal cavity. Most -of them did not developed true rostral ridges but have strongly upturned anterior margins af the !platform. The platforms are usua[ly ornamented, particularly so on the inner side w'ithinter rupted ridges or closely spaced nodes ar-ranged in rows. Occurrence. - Samples ooNected -by Kla:pper (Sandberg & Klapper 1967, p. B4.6)at Honnetal show the lowest occurrence of S. duplicata s. s. in the lowermost part of the Siphonodella - trianguJ1us inaequalis Zone. Ziegler & Leuteritz, in Koch Leuteritz .& Ziegler (1970), record S. duplicata in Seiler from the Siphonodella - triangulus inaequalis Zone and Siphonodella - triangulus triangulus Zone. In the zonation used by Sandberg & Klapper (1970), the first finding of S. du plicata mar'ks the base of the Siphonodella sa'lldbergi. - S. duplicata Zone. AccordIng to COllinson, Rexroad & Thompson (1971, Fig. 3), the ran,ge 0If the species reaches the Lower ChouteauFonnation 1= Siphonodella quadruplicata - S. crenulata Zone] in the northern Midcontinent of North America. Siphonodella lobata (Branson & Mehl, 1934) (PI. 6, Figs 11-12) 1934b. Stphonognathus tobata n. sp.; Branson & Mehl, p. 29'7, PI. 24, Figs 14-15. 1969. StphonodeUa tobata (Branson & Meh1); Rexroad, pp. G-44, Pt 2, Figs 5-8 [synonymy given]. 1969. SiphonodeUa tobata (Branson & Mehl); Schonlaub, p. 1345, Pt 2, Fip 11-12. 1970. S1.phonodeUa tobata (Bl"anson &: Mehl); Thompson & Fellows, p. 107, PI. 7, Figs 2, 4. Remarks. - The specimens in hand oonform with the holotype of Branson & Mehil. 'and Klapper's diagnosis (1966, p. 16), ex'cept for the lack of the secondary keel on the lower side of the outer lateral lobe. The main keel .is also less distinct then in most of the previously illustrated specimens, but more typical of the genus. This character relates the specimens with SiphonodeZla dupZicata from which S. Zobata probalbly developed (cf. Klapper 1966, p. 17). Occurrence. - Voges (1959, Tab. 1) records the range of SiphonodeZla lobata in Sauerland from the SiphonodeUa - triangulus triangulus Zone to the Lower (or Upper) Siphonodella crenulata Zone. Such a range of this SlpeCies lis confirmed by Schonlaub (1969, Tab. 1) :in ,the Camic Alps. I'll North America (Canis, p. 549, Tab. 3; Collinson, Rexroad & Thompson 1971, Fig. 3). S. lobata ranges from the Siphonodella sulcata Zone to the Siphonode1la ere!Ilulata - S.quadruplieata Zone. Siphonodella obsoleta Hass, 1959 (PI. 6, Fig. 9a-b) 1959. Stphonodetta obsoteta n. sp.; HlaSS, pp. 392-393, PI. 47, F>igs 1-2. 19'7J.. Stphonodetta obsoteta HBBSj K11llPPel", p. 12, Plo I, Fl.g. 25 [sYll!Onymy given]. Remarks. - The specimens investigated are small juvenile forms. In having only incipiently omamented platform, except for two rostral ridges, they ,are similar to SiphonooeUa cl. S. is08ticha (sensu Klapper 1971) but a leng ;rostral ridge that extends nearly to the posterior end of the outer platform is a diagnostic character of S. oosoleta. Occurrence. - Voges (19,59, Tab. 1) reoords S. obsoleta in Sauerland from the Siphonodella - triangulus inaequalis Zone to the Scaliognathus a'll-chorailis Zone. In NEPTUIDAN ])YKES AND THEIR CONODONT FAUNA FROIM DALNIA 51 the northern Midcontinent of North America (Collinson, Rexroad & Thompson 1971), the species range from the Siphonodella duplicata Zone through the Siphonodella isosticha - S. cooper! Zone. Siphonodella quadruplicata (Brnnson & Mehl, 1934) (PI. 6, Figs 6-7) 1934b. StphonognathuB quadrupUcata ID. Bp.; Bra.nson & Mehl, pp. 295--1.198, PI. 24, Figs 18-20 [non Fig. 21 = s. coopmi]. . 1966. StphonodeUa quadrupUcata (Branson & Mehl); Klapper, pp. 17-48, PI. 2, Flg.s ~; PI. e, Figs S-1IS; Pl. 4, FJgs 18, 20 J[sYlIJiQD.ym.y to 11166 glven]. 1968. stphonodeUa dupltcata (BrsIlSW1 & Mehl); C8Jlis, pp. 548-549, PI. 7Ia, Figs 3-4 [IIJOIIl F'1g. 7 = S. du.pttcata]. 1971. SlophonodeUa quadrupttcata (BraIlSOll & Meh1); KI~per, p. 12, PI. 1, Figs 22-U {synony my gtven]. Remarks. - The material a~ble consists of rather sman specimens having two or three rostral ridges. The specimens comparable with the same number ,af rostral it'idges, formel'ly designated as S. duplicata Val". A of Hass (1956), have been interpreted by Klapper (1966, p. 18) as early growth stages of S. quadrupticata. OCCUTTe(nCe. - The oorrect range of S. quadruplicata in Europe is not clear becaUSe of changes in concept of the SlPecies. Schon[aUlb (1969, Tab. 1) found it in the SiphonodeJ1a - trdangulus triangulus Zone and in the Siphonodella crenulata Zone of the Carnic Alps. In North America, Sandberg & Klapper (1967, p. B55) noted the lowest position of S. quadruplicata in the upper (part of the Siphonodella sandlbergi - S. duplicata Zone. CanIis (1968, Tab. 3) records it in Missouri from the Siphonodella sulcata Zone to the Siphonodella iisos1i.icha -S. oooperi Zone. Druce (1969, p. 122) records this species in Australia !from the 10wermost part of the Siphonociella quadruplicata - S. cooperi Zone. Siphonodella 8ulcata (Huddle, 1934) (PI. 6, Figs 1-2) 1934. PotygnathuB sutcata n. sp.; HlUddle, !p. 101, PI. 8, Fj,gs 23-23. 1962. StphonodeUa 8utcata (Huddle); Col1ilIlSOll, 8ClOtt & ReXTOad, Chart 2. 1968. StphonodeUa sutcata (Huddle); 0einitI, pp. 550-<551, PI. 'T.2, Fig/! 5, 22, 23. {non] 1969. Sitphonodena 8utcata (Eluddile); Druce, tJp. 122-;123, PI. 39, Fig. 1a-b [= S. dupUcata] • . 11969. SiphonodeUa sutcata (Huddle); Sch6n1aub, .p. 348, PI. 2, FJ.gs 18-40. 1969. S'tphonodeUa dupUcata (BrBiIlBOOl & Mehl); iRexroad, p. 43, PI. 2, Fig. 13. Remarks. - This speCies of SiphonodeUa !is characterized by an only incipiently developed rostrum. It is only marked by slightly upturned margin'S oIf the platform in its anterior part, but 'true rostra[ ridge's rnIIlning pa1"a1i1el to '1Jhe carina are not dev·eloped. The upper S'w.-faee of the ,platform is covered with ridges, but it may be also ornamented partly with nodes arranged in rows. This 'spec:les is closely a.-elated to the 'genus PoZygnathus, but the ~ack ofa definite basa[ cavity indicates that this species shoU[d .be placed in Siphonodetta (cf. Canis 1968, p. 551). Specin1ens designated by SchOnlaub (1969) as S. sulcata are here included into this species With reservation as having polygnathid aspeCts of the lower surface. The differences between S. sulcata and S. dupticata - see remarks on the latter. The differentiation between the two species is, however, strongly arbi'traTY. Occurrence. - S. sulCata have not been described by Voges (1959) from Sauerfland, but Klapper found it at HOnnetru railroad cut in the Protognathodus MICHAt. SZULCZEWSH;I kockeli - Pseudopo.lygnathus dentilineatus Zone (Sandberg & Klapper 1967, p. B46). It occurs in Wyoming and Montana in the Siphonodella sulcata Zone and it is rare in the llower part of Siphonodella sandbergi - S. duplicata Zone (Sandberg & Klap per 1967). Canis (1968, TaIb. 3) records this speCies in Missouri fro.m the Gnathodus sp. B (= Protognathodus kuehniZiegller & Leuteritz, 1970) - P. kookeli Zone to the lower part of the Siphono.deLIa quadruplicata - crenulata Zone. Genus SPATHOGNATHODUS Branson & Mehl, 1941 (Type spedies: Ctenognathus murchisoni Pander, 1856) Spathognathodus costatus costatus(Branson, 1934) (PI. 2, Figs 3-4) 1934. Spathodus costatus n. &p.; BTIallSon, p. 1303, PI. 27, Fig. 13. 1962. Spathognathodus costatus costatu8 (BraJll8O!l); Z!egler, pp. 107-.108, PI. 14, FIgs 1~, 8--10 ,[synonymy given]. 1964. Spathognathodus costatus C08tatus (Branson); Hdggi.ns, in HiggLns, Wa.gn.er-GentLs & Wa'gner, PI. 5, ll'ig. 31. ' " 1968. Spathognathodus costatus c08tatu8 (BTanson); lI/Lanzoni, p. 465, Pl. 60, Fdga 11-12. 196'1. Spathognathodus costatu8 oostatus (BrlllIlSon); van BoQgaert, pp. 186-167, PI. 3, Fip 20,22. 196'1. Spathognathodus c08tatus c08tatu8 (Bra.n801l); WoJsk.a, p. 4'J.6, PI. 19, F'igII .....12. [non] 1968. Spathognathodu8 c08tatu8 c08tatus (Braneon); Druce, p. 126, PI. 29, Fdgs 3-4. 1969. Spathognathiodus costatus c08tatus (BraJIl8Oll,); Ollviel"ii, pp. 81-&1, PL 12, Fig. 4a...... b; Pl. 26, FigB 7~. [non] 1969. Spathognathiodus costatu8 c08tatus (Branson); Rhodes, AUBtIin & Druce, p. 225, pI. 3, Figs 13-.15. ,1969. Spathognathodus btschofft n. lip.; Rhodes, Austin & iDruce, ,pp. 2~4, Pl. 4, Figs 1-4. Remarks. - According to. Ziegler (1962), p. 108) and some'subsequent autho.rs (see Sy>nOlIlymy), Spathognathodus costatus costatus is confined to. the Spatho.gnatho d1is CIOStatus Zone of the Upper Devonian -and maybe to the lower part of the Gatten:dorfia Zone (VOges 19,59). However, Rhodes, Austin & Druce (1969) and Druce (1969) found very simiaar specimens within conodont zones of the Avonian and in Bonaparte Gulf Bas'in (AUStralia), probably 'correlatable with the upper part of cu IIa 'and C'U IIP-r. Rhodes :& al. (l.c.) considered them as S. costatws costatus (Bransan) and induded aM. the Upper Devonian forms formerly described as this species in a neWly erected s.pecies S. bischaffi. These two taxa are regarded as ~. ho.meo.mortphic forms. These 'are, however,some doubts if the holotype of Branson actually conforms with S. oostatus costatus sensu Rho.des & al (1969) and not with the form desi'gnated by the latter as S. bischof/i. Branson's holotype was found in the Hannibal Formatio.n o.f Missouri, an equlrva'lent of cu I except for its uppermost part (cf. Canis 1968, Tab. 3). The locus typicus of S. costatus does not cor.respond 'With an interval comprising S. costatus costatus sensu Ziegler (1962) .[= S. bischoffi] or S. costatus c08tatus sensu Rhodes & al., ibut it falls within the intermediate interval. In addition, Prof. W. Zieg1er and Dr. Oh. Sandberg (written communication oi Prof. W. Ziegler 1972) a!fter examining the holotype of S. costatit.s and comparing'it with S. costatus costatus sensu Zieg,ler (1962) couLd not find any significant ctifferences between them. Consequently, the ooncept of S. costatus costatus sensu Ziegler (19132) is accepted here temporarily and the forms designated as the same species by Rhodes & al. (1969) are excluded from the syno.nymy of S. costatus costatus. The taxonomi<: P!9blem !presented a:bove ramains open until types will be scrutinized and compared in detala. The specimens in hand are closely 'COlllparable with the forms from the Upper Pevon~al'1: and differ from S. c08tatus costatus s'ens-u Rhodes & al. .(1969). The last- NEPTUNI'AN DYKES AND THEIR CONODONT FAUNA FROM DALNIA53 -named have nearly symmetrical, narrower and elongated basal cavity which is asymmetri'cal, wider in its anterior part and abruptly tapering posteriorly in S. costa tus costatus sensu Ziegler (1962). Occurrence. - See remarks. Spatihognathodus costatus spinulicostat'us (Branson, 1934) (PI. 2, Figs 1-2, 5) 1934. SpathoduB spinuUcoBtatus n. sp.; Branson, p. 305, PI. 27, Fig. 19. 1982. Spathognathodu8 c08tatuB spinultcostatus (Bra1lSOll); Zdegle.r, pp. 108--108, PI. 14, Figs 11- 18 l[synonymy given]. 196'1. SpQthognathodus costatus spinultcostatus (Branson); van Boogaert, p. 187, PI. 3, Fig. 25. 196'1. SpathognathoduB costatus spinultcostatuB (Brtanson); WoLska, p. 427, PI. 19, Fdgs 13~6. 1967. Spathognathodus costatuB spinultcostatus (Bramson); tSpasov & Fllipovd6, p. 80, PI. 4, Figs 1-4 ,[non Fdg. 3 = S. C08tatus costatus]. -[non] 1968. Spathognathodu8 costatus spinultcostatus (BraIlllOn); Ca,nis, p. 552, PI. 73, Fig. 15. 1969. Spathognathodus c08tatus spinuttcoBtatus (Bllanson); Old.vderl, p. 145, PI. 12, Fig. 7; PI. 26, Fdgs g....,10. 1969. Spathognathodus . costa tUB spinuttc08tatus (BraJllBOIl); &:h6n1aub, p. 348, Pt 3, Fig. 19. Remarks. - Rexroad, Austin & Druce 1(1969) included all the Upper Devoman specimens, formerly assigned to Spathognathodus costatus spinulicostatus, in the newly erected species S. ziegleri. They regarded .the last-named as a junior subjective synonym of S. sulciferus which they considered to be a subspecies of S. costatus. According to Rexroad & aa. (1969), S. costatus sulciferus lis confined in the Avonian to the <:'Ollodont zones, probably correlatable with the upper part -of cu IIa and cu IIP-r. However, the holotype of S. spinulicostatus differs from the holotype of S. sulciferus espeCially in the outline of the basa:1 cavity. Some undoubtly Upper Devonian ISpecimens (e.g. Wolska 1967, iPIl. 19, Fig. 16) closely resemble Branson's holotype of S. spinulicostatus in the ornamentation of upper sUrlface. Unfortunately, the outline of the bas'aiJ. oa'Vliiy of the holoty>pe (Branson 1934, Pl 27, Fig. 19) is not fuillly exposed on the illustration. Not haVling an oportunlty to see the type material of any species under study the writer does not !present definite conclusions, but until hDlotypes ·are scrutinized in detaH he is inclined to regard S. costatus spinuUoostatus sensu Ziegler (1962) as a valid and disinct SUbspecies. All specimens investigated fall within the range of variability of the subspecies. Occurrence. - Ziegler (1962, Tab. 2; 1971, Chart 6) records the range of the subspecies from the Lower (ex:cept foQl.' the lowermost part) to the Upper Spatho gnathodus costatus Zone. Spathognathodus disparilis (Branson & Mehl, 1934) {PI. 1, Fig. 7a-b) 1934a. Spathodus disparlZis'Il. lIP.; BrMlSOll & Mehl, pp. 189-190, PI. 17, Fig. 18. 11957. Spathognathodu8 dtsparittB (Branson & Mehl); Cloud, BaTnes & HaSIs, p. 809, PI. 5, Fig. I. ?l959. Branmehta d'isparlZis (BraDSOn &. Mehl); RaaI, p. 381, Pl. 50, Fig. 6 [the same specimen as that dHustrated by Cloud, BaTnes & HmIS 1957]. Remarks. - The dllustrafletd specimens of Spathognathodus disparilis available displays short andexceptiona:Lly wide ilateral extensions, otf whi'ch the inner is conspi cuously shorter than the outer. The upper surface of the outer extension bears two isolated nodes and on:ly one low node occurs on the upper surface of the inner extension. The blade is neal"ly straight. . Only two ' specimens previou&ly :illustrated have been 'assigned to Spathognat hoous disparilis. The specimen illustrated dilffers from the holotypeof &anson & 54 MICHAl. SZULCZEWSKI Mehl in a nearly stra1ght blade, which in the holotype :is curved more laterally. In contras1;to the iNustrated specimen, the upper surface of the inner extension in the holotype and in 'the second specimen in hand is unornamen'ted. The specimen iJ!Lustrated iby C1.oud, Bal['nes & Hass (1957) has an u.oornamented i\lpper Si\lrlace of bofu extensions and for this reason it is placed in the synonymy of the species with reservation. Spathognathodus dispariUs is a homeomorph of S. sannemamni Bischoff & Ziegler. A fewsulbspecies af the latter were erected by Pollock (1968) on the basis of differences in the OI['namentation of the lateral extentions. The division on the same basis of S. disparilis into sUibspecies may also be pos'sible, but this requires a richer material. Occurrence. - Hass (1959, p. 381) records S. disparilis in the Chappel Limestone, but it is ,considered to have been redeposited, as its actual range is believed to be a high Upper Devonian. Institute of Geology of the Warsaw University War8zawa 22, Al. Zwirki i Wigury 93 Warsaw, OctobeT 1972 REFERENCES ANDERSON W. I. 1966. Upper Devonian conodonts and the Devonian-Mississip.pian boundary of IllOrth-centra~ Iowa. - J. Paleont., vol. 40, no. 2. Chicago. - 1969. Lower MiSl3iS'Sippian canodon'ts from northern Iowa. - Ibidem, val. 43, .00. 4. ' AUSTIN R., CONlL R., RHODES F. & STREEL M. 1970. Conodontes, spores et ioraminiferes du Tournaisien ilnferieur dans la vallee du Hoyoux. - Ann. Soc. Geol. Be1g., vol. 93, fasc. 2. Bruxelles. BENDERP. & at (Arbellsgemefnschaft fUr Dinant-Stratigraphie). 19'11. Die strati graphische Gllederung des Dinantiums und seiner Ablagerungen in Deutsch [and. - Newsl Stratigr., vol. 1, no. 4. Leiden. BISCHOFF G. 1957. Die Conodonten-Stratigraphie des rheno-herzynischen Unter karbons mat Beriicksichtigung der Wocklumeria-Stufe undder Devon/Karbon -Grenze. - Abh. Hess. Landesamt BodenfOl['sch., H. 19. Wiesbaden. & ZIEGLER W. 1956. Das Aiter der "Urfer Schichten" im MarbUTger Hinterland , nach Conodonten. - Notizbl. Hess. Landesamt Bodenforsch., Bd. 84. Wiesbaden. BOOGAERT, ANDRICHEM H. A. van. 1967. Devonian and Lower Cal'lboiniferous oonodonts of the Cantabrian Mountains (Spain) and their stratigraphic apPli cation. - Leidse Geol Mededel, vol 39. Leiden. BRANSON E. B. 1934. Conodonts from the Hannibal Formation of Missouri. - Missouri Univ. Studies, vol. 8, .00. 4. Columbia, Miss. & MEHL M. G. 1934a. Conodonts from the Grassy Creek Shale af Missouri. - Ibidem, vol. 8, no. 3. 0& - 1934b. Conodonts from the Bushberg Sandstone and equivalent formations of Missouri - Ibidem, vol 8, no. 4. BUDUROV K. & TSCHUNEV D. 1964. Conodonten fauna und petrog.raphische Cha rakteristik der Gerollen aus den devonische und unterkarbonischen KaIlkste iDen in derm jungen Paleozoi Nord west bulgariens Itn Bulgarian]. - Bull. lost. Scient. de Recherche Geol., vol. 1. Sofia. CANIS W. F. 1968. Coniodonts and biostratigl['aphy of the Lower Mississippian of Mi1lSOuri. - J. pmeont., vol. 42, no. 2. Menasha. NEPTUNI'AN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 55 CLOUD P. E., BARNES V. E.Jr. & HASS W. H. 1957. Devonian-MissiSS'.ippian tran sition in central Texas. - BU!ll Geol. Soc. Amer., vol 68, no. 7. Baltimore. COLLLNSON C., REXROAD C. B. & THOMPSON T. L. 1971. Conodont zonation of the North American Mississippian. In: W. C. Sweet & S. M. Bergstrom ,(Eds.), Symposium on conodont biostratigraphy. - Geol. Soc. Amer., Mem. 127. , SCOTT A. J. & REXROAD C. B. 1962. Six charm sh KLAPPER G. 1966. Upper Devonian and Lower Mississippian oonodQnt :rones in Montana, Wyoming and South Dakota. - Univ. Kansas Paleont. Contr.• Paper 3. Lawrence, Kansas. 1971. Patrognathws and SiphonodelZa (Conodonta) from the Kinderhookian (Lower Mississippian) of western Kansas and southwestern Nebraska. - State Geol. Surv. Kansas, Bull. 202, Part 3. Lawrence, Kansas. , SANDBERG C. A., COLLINSON C., HUDDLE J. W., ORR R. W., RICKARD L. V., SCHUMACHER D., SEDDQN G. & UYENO T. T. '19'7'1. North Amen·can Devonian oonodont ibiostra'tigraphy. In: W. C. Sweet & S. M. Bergstriim (Eds.), Symposium on oooodonlt ibiostI'laUgraphy. - Geol. Soc. Amer., Mem. 127; KOCH M., LEUTERITZ K. & ZIEGLER W. 1970. Alter, Fazies und PaUiogeographie der OberdevonlUnterka:rfbon-Schichtenfolge an ' der Seiler ibei Iserlohn. - Fortschr. Geol. Rheml u. Westf., Bel 17. Krefeld. KREBS W. 1964. Zur faziellen Deutung von Conodonten-Mischfaunen. - Sencken berg. Leth., Bd. 114. Frankfurt a.M. 1971. Devonian reef limestones in the eastern Rheinish Schiefergebirge. - Sedimentology of parts of Central Europe. Guidebook. VIII Intern. Sediment. Congress 1971. KRYSTYN L., SCHAFER G. & SCHLAGER W. 1971. 'Ober die Fossil-LagersUi.tten in den triadi'schen lHalls'tiitter Kalken der Ostalpen. - N. Jb. Geol. PaUiont. Abh., Bd. 137, H. 2. Stuttgart. LINDSTROM M. 1964. Conodonts. Elsevier Publishing Company. Amsterdam. MANZONI M. 1966. COOlodonti neodevQnici ed eocarooniferi a,l Monte Zermula (Alpi · Camicbe). - GiQrn. Geol, serie 2a, vol. 33, fasc. 2. Bologna. - 1968. n DevonianQ superiore e il Carbonifero inferiore nelle serie pelagiche di Val Uqua (TarvisiQ). - Ibidem, VQI. 34, fasc. 2. MATTHEWS S. C. 1969a. A Lower CarboniferQus conodont fauna from East Cornwa.]J. - Palaeontology, vol. 12, part 2. London. - 1969b. Two conodont faunas from the Lower Carfoniferous .of Chudleigh, South Devon. - Ibidem. MATYJA B. A., MATYJA H. & SZULCZEWSKI M. 1973. The genus Eocaudina Martin (Holothuroidea) from the DeVlonian of Poland. - Acta Geol. Pol., VQl. 23, no. 1. W'arS'Zawa .. MOUND M. C. 1968. Upper DevQnian conodonts from Southern Alberta. .:.... J. Paleont., vol 42, no. 2. Menasha. OLIVIERI R. 11969. Conodonti e zonatura del Devoniano superiore e riconoscimento di Carbonifero inferiore nei calcari di Corona Mizziu (Gerrei - Sardegna). - BoIl. Soc. Paleont. Italiana, vol. 8, tIlO. 2. Modena. OSMOLSKA H. 1962. E'amennian a'lJ,d LOwer Carboniferous Cyrtosymbolinae (TriJ.o bita) from the Holy Cross Mountains, Poland. - Acta Palaeont. Pol., vol. 7, no. 112. Warszawa. 1973. Toumaisian trilobites from Damia in .the Holy Cross Mts. - Acta Geol. PoOl., vol. 23, no. !. Warszawa. PAPROTH E. & STREEL M. 1970. COirr~Hations biostratigraphiiques pres de la limite DevonieniCarlbonifere entre les facies littoraux al'dennais et les facies bathyaux rMnans. In: "Colloque 1Nll' la stratigraphie du Carbonifere". - Congres et oolloques Univ. Liege, vol. 55: Liege. POLLOCK C. A. 1968. Lower UiPper Devonian oonodonts fi'OIn Alberta, Canada. - J. Paleont., vo!. 42, 00. 2. .Menasha. REXROAD C. B. 1969. Conodonts from the Jacobs Chapel Bed (Mississippian) of the New Albany Shale in Southern Indiana. - Indiana Geol Survey Bull. 41. Bloomington. NEoPl'UNIAN DYKES AND THEIR CONODONT FAUNA FROM DALNIA 57 & SCOTT A. J. 1964. Conodont zones in the RoCkford Limestone and the lower ,part of the New Providence Shale (Mississippian) in Indiana. - Ibidem, Bull. 30. RHODES F. H. T., AUSTIN R. L. & DRUCE E. C. 1969. British Avondan (Carboni ferous) conodont faunas, and their value in local and interoontinental corre lation. - Bu:ll. Brit. Mus. Geology (NatlH". Hist.), Suppl. 4. London. ROZKOWSKA M. 1968. Famennian corals from the southern Holy Cross Mountains. - Intern. Symp. on the Devon:ian System, Alberta Soc. Petrol. Geol, vol. 2. Calgary. 1969. Famenruan tetracoralloid and heterocaralloid fauna from the Holy Cross Mountains, Poland. - Acta Palaeont. Pol., VIOIl. 14, no. 1. Warszawa. SANDBERG C. A. & IKLAPPER G. 1967. Stratigraphy, age, and paleotectcmic signi ficance oaf the Cottonwood Canyon Member of the Madison Limestone in Wyoming and !Montana. - U. S. Geol. Survey Bull. 1251-B. Washington. SCHLAGER W. 1969. Das Zusammenwirken von Sedimentation und Bruchtektonik in den triadischen Hallstatterlmlken der Ostalpen. - Geol. Rundschau, Bd. 59, H. 1. Stuttgart. SCHONLAUB H. P. 1969. Conodonten arus dem Oberdevon und Unterkarbon des Kronhofgrabens(!Karnische Alpen, Os'terr'eich). - Jb. Geol. Bundesanst., Bd. 112. Wien. SCHOLL W. U. & WENDT J. 1971. Obertrdadische und jurassische Spaltenfilllungen im Steinernen Meer (Nordliche Kalkalpen). - N. Jb. Geol. Palliont. Abh., Bd. 139, H. 1. Stuttgart. SCHULZE R. 1968. Die OOnOdonten aus dem Paliiozoikum der mittleren Karawanken Seeberggebiet. - Ibidem, Bd. 130, H. 2. SCHUMACHER D. 1971. Conodonts and .biostratigraphy of the "Kenwood" Shale (Upper Devonian). In: D. L. Clark (Ed.), Conodonts and biostratigraphy of the Wisconsin Pa1eozoik. - University Wisconsin, Inform. Circ. 19. MadLson. SCOTT A. J. & COLLINSON C. 1961. Conodont faunas f!l"om the Louisiana and McCraney Formations of Illinois, Iowa, and Missouri. - Guidebook, Kansas Geol. Soc. 26th Ann. Field Conference. SPASOV C. 1965. Unterkarbon in Bulgarien. - Rev. Bulgaria Geol. Soc., 26. Sofia. & FILIPOVIC I. 1967. Devondan and Carboniferous conodont fauna f.rom North-Western Ser'bia(yugOSllaV'ia) ,[in BuZgarian with EngZish summary]. - Izv. Geol. Inst., Ser. Paleont. (Bull. GeoJ.. Inst., Ser. Paleontology), val. 16. Sod'ia. STASINSKA A. 1973. - Tabulate corals from Dalnia in the Holy Cross Mts. - Acta Geol. Pol., vol. 23, no. 1. Warszawa. STOPPEL D. 1970. Die Fauna des Karbons 'Vom Djebel .A!bd-el-Aziz (Nordost-Syrien). 3. Oonodonta. - N. Jib. Gaol Palaont. Abh., Bd. 135, H. 2. Stuttgart. STRAKA J. J. 1968. Conodont zonation of the Kinderhookian Series, Washington County, Iowa. - Univ. Iowa Studies Natur. Hist., vol. 21. . STURANI C. 1971. Ammonites and stratigraphy of the "Posidonia alpina" beds of the Venetian Alps (Middle Jurassic, mainly Baj·oclan). - Mem. Inst. Geol Miner. Univ. Padova, vol. 28. Padova. SZULCZEWSKI M. 1971. Upper Devbnian 'conodonts, stratigraphy and facial develop ment!in the Hilly Cross Mts. - Acta Gaol. Pol., VIOL 21, no.!. WarszaJWa. THOMPSON T. L. 1967. Conodont zonation od' Lower Osagean rocks (Lower MissIs sippian) of soutwestern Missouri. - !Missouri Geol. Survey & Water Resources, Rept. Inv. 39. Rolla, Missouri. & FELLOWS L. D. 1970. Stratigraphy and oonodont hiostratigraphy of Kinder hookian and Osagean rocks of southwestern Missouri & adjacent areas. - Ibidem, Rept. Inv. 45. 58 MICBAl. SZULCZEW'SKI VOGES A. 1959. Conodonten aus dem Unterkarbon I rund 11 (Gattendor/ia- und Pe ricyclus-8tufe) des SauerLandes. - PaUiont. Z., Bd. 33, H. 4. Stuttgart. WEND'!' J. 1971. Genese und Fauna submariner sedimentarer Spaltenfullungen im Mediterranen Jura. ·- iPalaeontographica, Bd. 136, Aht. A. Stuttgmt. WEYER D. 1965. Etroeungt Un Morvan (Zentralfrankreich). - Mlttellungen ZGI, H. 1. Berlin. 196'1. Zur strafigraphischen Verbreitung der Heterocorallia. - Jb. GooI., Bd. 1. (1965). Berlin. 1971. Neaxon regulus (Rh. Richter, 1848), ein Lel.tfos.sil der mitteleuropaischen Wocklumeria-StuJfe {Anthozoa, Rugosa; OberdevoQll). - Geologie, Bd. 20, H. 3. Berlin. WOLSKA Z. 196'7. Upper Devonian conodonts from the south-west region of the Holy Cross MOUIDtaimI,PoJand. - Acta Palaeont. Pol., VIOl. 12, DO. 4. Warszawa. ZANKL H. 1971. Upper Triassic carbonate facies in the Northern Limestone Alps. - -'- Sedimentology of parts of Central Europe. Guidebook. VIII Intern. Sediment. Congress 1971. ZIEGLER W. 1962. Taxionomie nod PhyLogenie Oberdevonischer Conodonten und lMe stratigraphische Bedeuttmg. - Albh. Hess. Landes'amt Bodenforscll., H. 38. Wieslbaden. 1969. Eine neue Conodotenfauna aus dem hOchsten Oberd·evon. - Fortschr. Geol. Rheinl. 'u. Westf., Bd. 17. Krefeld. 1971. Cooodont stratigraphy of the European Devonian. In: W. C. Sweet & S. M. Bergstram (Eds.), Symposdum on oonodont biostratigraphy. - Geol. Soc. Amer.., Mem. 127. ZAKOWA H. 1967. The Lower carboniferous from the vici.nity of BoJ.echowice, Holy Cross Mts. - Acta Geol Pol., vol. 17,00.1. Warszawa. 1970. The present state of the stratigraphy and paleogeography ,of the Car boniiferous in ,the Holy Cross Mts. - Ibidem, vol. 20, no. 1. M. SZULCZEWSKI FAMElQ"SKO-TURNEJSKIE Zn.,y NEPTUNICZNE Z FAUN" KONODONTOWl\ NA DALNI W OORACB S~OKRZYSKICB (Streszczenie) Przedmlotem pracy jest anailiza sedymentoLogiczno-facjalna oraz stratygraficz na zyl nepttmiamych {tj. osad6w, kt6.re w warunkach podInorskich wypebilly syn sedymentacyjne szcze1iny tektoniczne), wystlS>ujl\cych na wzg6r~u Daln:ia kolo Kielc (vide fig. 1-5), gdz.ie pr'Zecinajlt oQlle wapienie oolitowe W1ieticzl\ce pram fl'anu (por. Szulczewski 1971). Znalez'ione zyly neptuniczne zawierajl\ bardzo bogaty i u'llikalny zesp61 skamienialoSci, na kt6ry skladajlt si~ przede rwszystklim loo.ralowce, trylobity i konodonty, zas brachiopody, amonity i strzykwy stanowil\ element tOW8-"'Zyszl\cy. Szczeliny prowadzl\ce do utworzenia zyl byly kilkakrotn1e rozwierane i wypemiane w wmunkach podmorskich, a zawa.rta w obr~bie zyl fauna konodontowa wskazuje, ze NEPl'UNIAN DYKES AND THEIR CUNODONT FAUNA FROM DALNIA 59 procesy te zachodzily zar6wno w famenie jak i w t-urneju. Wypclnienie zyl odpowiacia skondensowanej sekwencji wapiennej osadzonej na grzbiecie podmorskim. Zrekon struowany zarys obszaru zwolnionej sedymentacji w famenie i w turneju zachod niej cz~ G6r Swi~tokrzyskich pokrywa si~ w przybliZeniu z zarysem obumadej franskiej rafy plytowej (poT. Szulczewski 1971); sedymentacja sekwencji skondenso wanej jest zatemtutaj zjawiskiem potomnym w stosunku do sedymentacji rafowej. Przebieg granic Ifacjalnycll w g6rnym dewonie i w turneju by} tutaj natomiast w znacznym stopniu wyznaczany przez r6wnoczesne z sedymentacjll dyslokacje blo kowe. Przedstawiona zmiennoSe facjama wydaje si~ miee takze wplyw na uksztalto wanie p6miejszydh (hercyiisitiCh) form te.ktonicznych, m. in. fald6w s1uchowickich i synkliny kieleckiej. W 'Cz~sci pa[eontologicznej pra'Cy opisano 29 gatunk6w i podgatunk6w kono dont6w (vide plo 1-6), gl6wnie turnejski1ch, lkt6re z obszaru G6r Swi~tokrzys'kich nie byly dotyCihczas apisy'wane. Pozostale gTUpy faunistyczne ro:z;patrzono w naw'ill za:niu do r6wnoczesnyoh opracowaii szczeg6lowyoh, poSwi~onych koralom denkowym (Stasiiiska 1973), cz~ci korali czteropromiennych (Fedorowski 1973) oraz trytloibitom (Osm61ska 1973). Caly !l'ozpatrywany zesp61 fauniatyczny, b~llcy najbogatsz~z do tyCbczars znanY'Ch w turneju G6r SWi~tokrzYSkich, zdaje si~ bye niepowtarzalnym z tego takZe wzgl~du, ze abszar Dalni jest jedynym, gdzie osady tUrnejsikie all niemal w caloSci wykszta1cone w facji wapiennej. Instytut GeoZogii Podsta'UJOlWej Uniwersytetu WaTBzawskiego Warszawa 22, Al. Zwirki i Wigury 93 WaTszawa, w pazdzierniku 1972 T. .1